U.S. Department of the Interior

U.S. Geological Survey

Pamphlet to accompany

Scientific Investigations Map 3280

Prepared in cooperation with the National Park Service

Bedrock Geologic Map of the Spring Valley, West Plains, 

and Parts of the Piedmont and Poplar Bluff 30'×60'

Quadrangles, Missouri, Including the Upper Current River

and Eleven Point River Drainage Basins 

By David J. Weary, Richard W. Harrison, Randall C. Orndorff, Robert E. Weems, J. Stephen Schindler, 

John E. Repetski, and Herbert A. Pierce
U.S. Department of the Interior

SALLY JEWELL, Secretary

U.S. Geological Survey

Suzette M. Kimball, Acting Director

U.S. Geological Survey, Reston, Virginia: 2014

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Although this information product, for the most part, is in the public domain, it also may contain copyrighted materials 

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Suggested citation:

Weary, D.J., Harrison, R.W., Orndorff, R.C., Weems, R.E., Schindler, J.S., Repetski, J.E., and Pierce, H.A., 2014, Bedrock geologic map of the Spring Valley, West Plains, and parts of the Piedmont and Poplar Bluff 30' × 60' quadrangles, 

Missouri, including the upper Current River and Eleven Point River drainage basins: U.S. Geological Survey Scientific 

Investigations Map 3280, 2 sheets, scale 1:100,000, and 55-p. pamphlet, http://dx.doi.org/10.3133/sim3280.

ISSN 2329-1311 (print)

ISSN 2329-132X (online)

ISBN 978-1-4113-3726-8

Cover. View looking downstream along Jacks Fork in the Jam Up Cave 7.5-minute quadrangle, 

Missouri. The Gasconade Dolomite crops out on the lower slopes of the bluff flanking the river and 

the Roubidoux Formation crops out on the upper slopes. The formation contact is about 100 feet 

above river level near the top of the cliff in the middle distance. As is typical of the upper parts of 

Jacks Fork and the upper parts of the nearby Current River, local flow tends to be in the direction of 

the dip of the bedrock, which here is toward the southeast. The small light-colored area on the cliff 

in the middle distance is a relatively fresh rockfall scar. Photograph by Victoria Grant, National Park 

Service, March 2007.
iii

Contents

Introduction.....................................................................................................................................................1

Previous Work .......................................................................................................................................2

Geologic Map Preparation..................................................................................................................3

Discussion.......................................................................................................................................................4

Stratigraphy ...........................................................................................................................................4

Paleoproterozoic Rocks..............................................................................................................4

Mesoproterozoic Rocks..............................................................................................................4

Mesoproterozoic Silicic Rocks.........................................................................................4

Mesoproterozoic Volcanic Ridge Beneath Hurricane Creek ......................................4

Mesoproterozoic Mafic Plutonic Rocks .........................................................................5

Proterozoic-Paleozoic Unconformity .......................................................................................5

Cambrian and Ordovician Geologic History ............................................................................5

Surficial Geology..........................................................................................................................7

Karst Geology ........................................................................................................................................7

Sinkholes.......................................................................................................................................8

Structural Geology................................................................................................................................8

Northeast-Trending Faults..........................................................................................................9

Northwest-Trending Faults.........................................................................................................9

Seismicity....................................................................................................................................11

Mississippi Valley-Type Base-Metal Occurrences..............................................................11

Fletcher Mine ....................................................................................................................12

Sweetwater Mine .............................................................................................................12

Audio-Magnetotelluric (AMT) Survey...........................................................................13

Hydrogeology ......................................................................................................................................14

Description of Map Units............................................................................................................................16

Paleozoic Sedimentary Rocks ..........................................................................................................16

Mesoproterozoic Intrusive Rocks....................................................................................................18

Mesoproterozoic Volcanic Rocks ....................................................................................................18

Upper Sequence of Mesoproterozoic Volcanic Rocks .......................................................18

Lower Sequence of Mesoproterozoic Volcanic Rocks ......................................................20

References Cited..........................................................................................................................................21

Appendix 1. Summary of Drill-Hole Data for the Study Area .............................................................27
iv

Tables

1. Geologic maps of 7.5-minute quadrangles in the study area that have been 

published to date at 1:24,000 scale by the U.S. Geological Survey ......................................2

2. Biostratigraphic determinations for Mississippian chert collections from 

the Current River drainage basin, Missouri .............................................................................6

3. Summary of high-grade base-metal mineralization encountered in drill holes 

in the Bonneterre Formation several kilometers north of Greer Spring, Mo. ...................12

Conversion Factors and Datums

Inch/Pound to SI

Multiply By To obtain

inch

inch

foot (ft) 

mile (mi) 

Length

2.54

25.4

0.3048

1.609

centimeter (cm)

millimeter (mm)

meter (m)

kilometer (km)

Area

square mile (mi2 ) 2.590 square kilometer (km2 )

Volume

cubic mile (mi3

SI to Inch/Pound

) 4.168 cubic kilometer (km3)

Multiply By To obtain

Length

centimeter (cm)

millimeter (mm)

meter (m)

kilometer (km)

0.3937

0.03937

3.281

0.6214

inch

inch

foot (ft)

mile (mi)

Area

square kilometer (km2 ) 0.3861 square mile (mi2 )

Volume

cubic kilometer (km3) 0.2399 cubic mile (mi3)

Temperature in degrees Celsius (°C) may be converted to degrees Fahrenheit (°F) as follows:

°F = (1.8 × °C) + 32

Vertical coordinate information is referenced to the National Geodetic Vertical Datum of 1929 

(NGVD 29).

Horizontal coordinate information is referenced to the North American Datum of 1983 (NAD 83).
Bedrock Geologic Map of the Spring Valley, West Plains, 

and Parts of the Piedmont and Poplar Bluff 30' ×60'

Quadrangles, Missouri, Including the Upper Current River 

and Eleven Point River Drainage Basins 

By David J. Weary, Richard W. Harrison, Randall C. Orndorff, Robert E. Weems, J. Stephen Schindler, 

John E. Repetski, and Herbert A. Pierce

Introduction

This geologic map covers the drainage basins of the 

upper Current River and the Eleven Point River in the Ozark 

Plateaus physiographic province, southeastern Missouri 

(figs. 1; 2A,B). The two surface drainage basins are contiguous 

in their headwaters regions, but are separated in their lower 

reaches by the lower Black River basin in the southeast 

corner of the map area. Numerous dye-trace studies that are 

summarized by Imes and Kleeschulte (1995) and Kleeschulte 

(2000) demonstrate that in the contiguous headwaters areas of 

the Eleven Point and Current Rivers, groundwater flows from 

the Eleven Point River basin into the Current River basin. 

Much of the groundwater discharge of the Eleven Point River 

basin emanates from Big Spring, located on the Current River 

(fig. 2A) (Aley and Aley, 1987; Imes and Kleeschulte, 1995). 

This geologic map and cross sections were produced to help 

fulfill a need to understand the geologic framework of the 

region in which this subsurface flow occurs.

In addition to depicting the geology of the study area, 

this map shows prominent linear anomalies in regional 

magnetic trends, derived from a residual magnetic field map 

(see figure 3) that was produced in 1996 by T.G. Hildenbrand 

of the U.S. Geological Survey (USGS) for this study. These 

anomalies are tentatively interpreted to be representative of 

faulting in basement rocks. This text pamphlet summarizes the 

regional geologic framework and highlights some of the more 

significant findings of this work. Additional detailed descriptions, data, and interpretations of karst features, hydrogeology, 

stratigraphy, Mesoproterozoic igneous and tectonic geology, 

audio-magnetotelluric surveys, and tectonics can be found in 

other publications produced during our study of the region 

(Lowell and others, 2010; Orndorff and others, 2006; Weary 

and Orndorff, 2001; Orndorff and others, 2001; Lowell and 

Harrison, 2001; Orndorff and others, 2000; Repetski and 

others, 2000; Harrison and others, 2000; Šebela and others, 

1999; Repetski and others, 1998). Published geologic maps of 

7.5-minute quadrangles produced for this study are listed in 

table 1 below.

This map includes all of the Ozark National Scenic 

Riverways (fig. 2A), a national park created by an Act of 

Congress in 1964 to protect 134 miles (mi) (216 kilometers 

(km)) of the Current and Jacks Fork Rivers in south-central 

Missouri. Located within the park are numerous large springs, 

including Big Spring, the largest spring in Missouri and one of 

the ten largest springs in the world.

Also within the map area is Greer Spring, which 

is the main source of the Eleven Point River that flows 

through the Eleven Point Unit of the Mark Twain National 

Forest (U.S. Forest Service) (fig. 2A). Greer Spring is the 

largest spring on National Forest land in the United States. 

During flood, flow from Greer Spring is almost as large, 

volumetrically, as that of Big Spring, making Greer Spring 

also one of the largest springs in the world. Acknowledging a 

44-mi (77-km) section of the Eleven Point River below Greer 

Spring as one of “certain selected rivers of the Nation which, 

with their immediate environments, possess outstandingly 

remarkable scenic, recreational, geologic, fish and wildlife, 

historic, cultural, or other similar values,” the Wild and 

Scenic Rivers Act in 1968 established the Eleven Point 

National Scenic River, which is entirely within the boundaries 

of this map (fig. 2A).

Potentially economic mineral resources are present in 

the subsurface in the map area. Exploration drill-hole data 

indicate that anomalously high concentrations of base-metal 

sulfides locally occur within the Cambrian Bonneterre 

Formation (see table 3). The geologic setting of these anomalous concentrations is similar to that found in the Viburnum 

Trend (Economic Geology, 1977), which is contained in the 

southeast Missouri lead mining district, the largest lead mining 
2 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Table 1. Geologic maps of 7.5-minute quadrangles in the study area that have been published to date at 1:24,000 scale by the

U.S. Geological Survey.

[Information on ordering published maps can be obtained by calling the U.S. Geological Survey at 1–888–ASK–USGS (1‒ 888‒275‒8747) or by visiting the 

USGS online at http://www.usgs.gov/pubprod]

Quadrangle name USGS map series

number

Reference

(see References Cited) URL for online access

Greer I‒2618 McDowell (1998) http://pubs.usgs.gov/imap/i-2618/

Eminence I‒2653 Orndorff and others (1999) http://pubs.usgs.gov/imap/i-2653/

Powder Mill Ferry I‒2722 McDowell and Harrison (2000) http://pubs.usgs.gov/imap/i-2722/

Winona I‒2749 Orndorff and Harrison (2001) http://pubs.usgs.gov/imap/i2749/

Stegall Mountain I‒2767 Harrison and others (2002) http://pubs.usgs.gov/imap/i2767/

Low Wassie I‒2719 Weems (2002) http://pubs.usgs.gov/imap/i2719/

Wilderness and Handy I‒2801 Harrison and McDowell (2003) http://pubs.usgs.gov/imap/i2801/

Fremont I‒2775 Orndorff (2003) http://pubs.usgs.gov/imap/i2775/

Van Buren North I‒2802 Weary and Weems (2004) http://pubs.usgs.gov/imap/i2802/

Van Buren South I‒2803 Weary and Schindler (2004) http://pubs.usgs.gov/imap/i2803/

Big Spring SIM 2804 Weary and McDowell (2006) http://pubs.usgs.gov/sim/2006/2804/

Cedargrove SIM 2980 Weary (2008) http://pubs.usgs.gov/sim/2980/

Piedmont Hollow SIM 2979 Weary (2008) http://pubs.usgs.gov/sim/2979/

Round Spring SIM 3073 Orndorff and Weary (2009) http://pubs.usgs.gov/sim/3073

Alley Spring SIM 3161 Weary and Orndorff (2012) http://pubs.usgs.gov/sim/3161/

Jam Up Cave and Pine Crest SIM 3248 Weary and others (2013) http://pubs.usgs.gov/sim/3248/

district in the world. The southernmost part of the Viburnum 

Trend (fig. 2A) extends into the northern part of the map area 

and is exploited by the Sweetwater Mine. Undeveloped and 

potentially economic occurrences of base metals are known 

also beneath Blair Creek (Kisvarsanyi, 1977; Hagni, 1989), 

which is a tributary to the Current River in the north-central 

part of the map area.

Previous Work

Few detailed geologic maps were available for much 

of the upper Current River basin or the Eleven Point River 

basin prior to this project.  A portion of the upper Current 

River basin was mapped at 1:62,500 scale during the 1920s 

by Bridge (1930), and the northern half of the upper Current 

River basin was compiled to 1:250,000 scale through reconnaissance mapping conducted mostly during the 1970s and 

1980s (Pratt and others, 1992). The geology of approximately 

30 mi2

 (78 km2) in and around the Irish Wilderness Roadless 

Area, Oregon County, was mapped at 1:24,000 scale 

by Heyl and others (1983) as part of a mineral resource 

potential map. Partly concurrent with field investigations 

for the present report, the Missouri Department of Natural 

Resources, Geological Survey and Resource Assessment 

Division, mapped three contiguous 7.5-minute quadrangles 

in the southeast corner of the study area (fig. 2A); they are 

Grandin SW (Baker, 1999), Briar (Starbuck, 1999), and Poynor 

(Wedge, 1999). After making some modifications we compiled 

the data from these three maps into the present report. Fisher 

(1969) and Sinha and Kisvarsanyi (1976) mapped parts of the 

Mesoproterozoic volcanic rock exposures on Stegall and Mule 

Mountains. A small, structurally complex area near the town 

of Thayer, located in the extreme south-central part of the map 

area, was mapped by Hedden (1968), and with some reinterpretations his mapping was incorporated into the final map. 

Miscellaneous unpublished reconnaissance geologic maps at 

various scales that provide coverage for various parts of the 

study area exist in the archives of the Missouri Department of 

Natural Resources in Rolla, Mo. A preliminary geologic map 

of the Spring Valley 30' × 60' quadrangle, which encompasses 

most of the upper Current River basin, was produced by 

Orndorff and Harrison (1997). 

Introduction
Introduction 3

Geologic Map Preparation

The majority of the field data and interpretations 

presented in this report were compiled and synthesized from 

prior, chiefly USGS, geologic mapping and field observations, 

which represent almost 15 years of effort. Compilation for 

this report includes both detailed data, at 1:24,000 scale, and 

reconnaissance data, collected at 1:100,000 scale. For the parts 

of the study area that were mapped by the USGS at 1:24,000 

scale, geologic contacts were identified and traced in the field 

and locations were determined by global positioning system 

(GPS) measurements and relations to topography. In areas of 

poor exposure, structure contours of individual stratigraphic 

horizons were drawn from observed point data, and contacts 

then were drawn to match equal-values intersections of the 

structure contours and topographic elevations. 

Table 1 provides a list of the 1:24,000-scale 7.5-minute 

geologic map quadrangles that have been published to date by 

the USGS and used in the preparation of this report. 

Data from all earlier geologic investigations in the study 

area, including dozens of unpublished field sheets on file at the 

Missouri Department of Natural Resources, Geological Survey 

and Resource Assessment Division, Rolla, were utilized in the 

preparation of this report. We drove the majority of roads in 

the reconnaissance area and collected geologic information 

from observed outcrops and float. Appendix 1 gives some of 

the drill-hole data that we incorporated into map preparation; 

in addition, we used well logs from a database compiled by 

the Missouri Department of Natural Resources, Division 

of Geology and Land Survey. Those logs are now available 

online at http://www.dnr.mo.gov/env/wrc/logmain/index.html. 

Most contacts in areas mapped by reconnaissance were drawn 

based on structure contours derived from limited outcrop 

and well data. 

Only a few of the faults shown in areas of reconnaissance 

mapping were directly observed in the field; most faults, 

therefore, are considered to be inferred and approximately 

located. Criteria used for establishing the existence and 

trend of faults include (1) continuation of faults from areas 

mapped in detail, (2) disruptions of regional stratigraphy, 

(3) stratigraphic offsets indicated by drill-hole data or by 

faults penetrated by drill holes, and (4) field evidence indicative of cataclasis. Juxtaposition of different geologic units, 

deformation bands in sandstone, tectonic brecciation, and 

slickensides were the most common types of fault evidence 

observed in the field and used in delineating the traces of 

faults in areas mapped in detail. Some inferred faults shown 

on the map are drawn on magnetic linear features (see figure 

3). Because of extensive vegetation and residuum cover and 

the overall paucity of exposures, intersections between two or 

more faults and crosscutting fault relationships portrayed on 

the geologic map are mostly interpretative. 

This report depicts prominent linear anomalies in regional 

aeromagnetic data derived from a compiled map of the 

residual magnetic field (fig. 3) produced by T.G. Hildenbrand 

(USGS, Menlo Park, Calif., deceased) in 1996 for this study. 

The compiled map followed earlier publication of statewide 

magnetic anomaly maps by the USGS (Hildenbrand and 

Kucks, 1991, 1992). Information on the source datasets and on 

procedures used to process and compile the data is available in 

a digital report by Kucks and Hill (2005). Both ground-based 

and aeromagnetic data were used in this compilation. The 

mapped magnetic data were examined independently of the 

geology and apparent linear anomalies were then drawn over 

it. Only those anomalies that do not coincide with mapped or 

inferred faults are shown on the final geologic map. 
4 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Discussion

Stratigraphy

The stratigraphic section in the map area comprises 

several thousand feet of nearly flat-lying Cambrian 

and Ordovician marine sedimentary strata that, with 

angular unconformity, overlie a basement of dominantly 

Mesoproterozoic igneous rocks. Some Paleoproterozoic 

metamorphic rocks could lie beneath the westernmost part 

of the map area (Sims, 1990), and some of the basal section 

of the Lamotte Sandstone could be as old as Neoproterozoic. 

Figure 4 shows a stratigraphic column for these rocks; see 

Lowell and others (2010) and the published geologic maps 

of the 7.5-minute quadrangles listed in table 1 for detailed 

descriptions of stratigraphic units. 

The Proterozoic-Paleozoic contact is highly irregular, 

and locally exhibits paleo-relief of as much as 1,600 feet (ft) 

(500 meters (m)) over relatively short distances (see cross 

sections), resulting in protrusions of basement rocks into 

the Paleozoic section. The study area has been subaerially 

exposed from as far back as the Cretaceous to the present, 

and during this period a relatively thick cover of residual 

and colluvial material was developed extensively on the 

Paleozoic sediments.

Paleoproterozoic Rocks

Paleoproterozoic metamorphic rocks may occur in the 

subsurface in the westernmost part of the map area (Sims, 

1990), but this is unconfirmed by drill-hole data. Sims (1990) 

ascribed these metamorphic rocks to the North American 

Paleoproterozoic crust that formed during the Central Plains 

orogen from ~1,800 to 1,600 Ma (mega-annum) (Sims and 

Peterman, 1986).

Mesoproterozoic Rocks

Mesoproterozoic Silicic Rocks

The Mesoproterozoic basement rocks consist principally 

of an older suite (~1.47 Ga) (giga-annum) of plutonic and 

volcanic rocks, and a younger suite (~1.38 Ga) of silicic, 

epizonal plutonic rocks (Sims, 1990; Van Schmus and others, 

1996). A cluster of more than 50 knobs of the older suite 

protrude through the Paleozoic section and crop out in the 

Current River basin; elsewhere, the older suite does not crop 

out and is known only from subsurface data. A subcrop map 

of the Proterozoic basement beneath the map area can be 

found in Lowell and others (2010, fig. 8.7). Detailed discussions on the geology and geochemistry of the outcropping 

Mesoproterozoic rocks can be found in Lowell and others 

(2010), Lowell and others (2005), Harrison and others (2002), 

Orndorff and Harrison (2001), Lowell and Harrison (2001), 

Harrison and others (2000), McDowell and Harrison (2000), 

and Orndorff and others (1999).

An important feature of the Mesoproterozoic basement 

within the map area is the Eminence caldera, first described by 

Kisvarsanyi (1977, 1984). The approximate limit of location 

of the caldera is shown in figure 3. Caldera fill consists 

of ignimbrites and lavas that are divisible into an upper 

sequence and a lower sequence. Lower sequence volcanic 

rocks, commonly exhibiting dips of 65 degrees (°) to 90° 

that likely reflect caldera collapse, have a probable thickness 

of 7 to 8 km and a volume of at least 360 km3. These rocks 

are overlain with angular unconformity by post-collapse, 

subhorizontal effusive rocks of the upper sequence that have a 

thickness of about 300 m. The unconformity is marked by an 

air-fall tuff at the base of the upper sequence, called the tuff 

of Mule Mountain. Lower sequence caldera-collapse rocks 

have been dated at 1,480±42 Ma (Van Schmus and others, 

1996) and post-collapse rocks have been dated at 1,470±2.7 

Ma (Harrison and others, 2000). The strike of rotated lower 

sequence caldera-collapse rocks displays a strong northwest 

trend (Lowell and others, 2010; Harrison and others, 2002; 

Orndorff and Harrison, 2001; Lowell and Harrison, 2001; 

Harrison and others, 2000); McDowell and Harrison, 2000; 

and Orndorff and others, 1999), which has been interpreted 

as indicating an inherent northwest-trending fabric in the 

basement. This fabric influenced caldera formation in a transtensional tectonic setting created by a left step in a left-lateral 

strike-slip fault system (Harrison and others, 2000; Lowell and 

others, 2010). From petrographic studies conducted elsewhere 

in southeastern Missouri, foliation-parallel left-lateral, 

northwest-trending ductile shear has been postulated for 

Mesoproterozoic-age basement rocks (Lowell and Clendenin, 

2003; Lowell and others, 1995; Diehl and others, 1995). A 

genetic link between magma emplacement and transtensional 

step-overs in strike-slip faulting has been long established in 

the literature (Hutton and others, 1990; Schmidt and others, 

1990; Glazner, 1991; Tikoff and Teyssier, 1991; and RománBerdiel and others, 1997).

Mesoproterozoic Volcanic Ridge Beneath Hurricane Creek

Deep drilling in the Low Wassie quadrangle (see 

appendix 1) in the vicinity of Hurricane Creek in Shannon 

and Oregon Counties has delineated a northwest-trending 

ridge on the Proterozoic-Paleozoic unconformity that is 

underlain by Mesoproterozoic volcanic rocks (fig. 5; cross 

section B–B'). This buried feature closely coincides with a 

geophysical magnetic anomaly identified by Spector (1982) 

and is indicated in figure 3. Deep drill-hole data further 

indicate that the buried Hurricane Creek volcanic ridge is 

separated from volcanic rocks within the Eminence caldera 

by plutonic rocks of Mesoproterozoic age. The Hurricane 

Creek ridge is offset dextrally by the northeast-striking 

Wilderness-Handy fault zone from another topographic high 

on the unconformity, which is also underlain by volcanic rocks 

(Spector, 1982). Although the attitudes of volcanic fabric of 

these rocks are unknown, the similarity between the trend 

of the ridge and the volcanic fabric observed in outcropping 
Discussion 5

volcanic rocks in the Eminence caldera strongly suggests that 

the volcanic rocks beneath Hurricane Creek have a steeply 

dipping, northwest-trending fabric. We further hypothesize 

that the buried Hurricane Creek volcanic rocks represent 

a distinct Mesoproterozoic volcanic center. An alternative 

hypothesis would be that the volcanic ridge is an outlier of the 

larger Eminence caldera, which either was eroded deep into 

its co-genetic plutonic equivalent or was intruded by younger, 

~3.8-Ga plutonic rocks. 

Mesoproterozoic Mafic Plutonic Rocks

The magnetic signature of mafic plutonic rocks that 

underlie the Eleven Point River basin (see cross section B–B′ ) 

in the northwestern corner of Oregon County, in T. 25 N., 

R. 6 W., creates a distinctive anomaly on the magnetic field 

map (fig. 3, white circle). This anomaly was drilled in 1968 

to 1970 by the American Zinc Co. as part of their exploration 

program for nickel, copper, and cobalt deposits. They drilled 

three holes, which encountered rocks of olivine gabbro, 

uralitic gabbro, and norite composition (Kisvarsanyi, 1975). 

Van Schmus and others (1996) reported an age of approximately 1,500 Ma for these rocks, which is similar to ages of 

most mafic plutons elsewhere in Missouri. From inspection 

of drill cores of mafic plutons in Missouri, Kisvarsanyi (1974, 

1988) described these bodies as differentiated layered intrusions that are typically intruded by granitic material and that 

contain disseminations of pyrrhotite, magnetite, pentlandite, 

and chalcopyrite. Van Schmus and others (1996) concluded 

that the mafic plutons are probably contemporaneous with 

the 1,470±40-Ma silicic igneous rocks, and that the magma 

source for the body beneath the Eleven Point River basin 

was probably Mesoproterozoic depleted mantle and perhaps 

juvenile subcontinental lithosphere.

Proterozoic-Paleozoic Unconformity

The unconformity between Proterozoic basement rocks 

and the overlying Paleozoic section is an erosional surface 

that represents more than 800 million years. During this long 

period of nondeposition, the supercontinent of Rodinia, which 

included the North America craton, was initially assembled 

between ~1,340 and 1,000 Ma. Basement rocks within the 

map area would have been within a few hundred kilometers 

of the orogenic front composing the southern margin of the 

North American plate (see Thomas, 2006). Therefore, we 

assume that some of the faulting observed in outcropping 

Mesoproterozoic sections is probably associated with largescale plate tectonic movements during this period.

Along the unconformity, volcanic rocks that were 

deposited at the Earth’s surface now lie at the same elevations as coeval plutonic rocks that cooled at depths in excess 

of 5,000 to 6,000 ft (about 1.5 to 2 km), thus indicating 

substantial pre-Paleozoic deformation, localized uplift, and 

subsequent erosion.

Cambrian and Ordovician Geologic History

A renewed depositional record of geologic history in the 

map area began during the breakup of Rodinia, which lasted 

from about 760 Ma to about 530 Ma (see Thomas, 2006), 

when syntectonic marine sediments were laid down beneath 

an epicontinental sea that occupied most of Midcontinent 

North America. The floor of a major crustal rift, which 

ultimately failed and became known as the Reelfoot rift, lies 

only 60 km to the southeast of the map area (see Hildenbrand 

and Hendricks, 1995). In the southeastern part of the map 

area subsurface, the Cambrian succession (the Bonneterre 

and Davis Formations of the Elvins Group) exhibits thickness variations and facies transitions that were controlled 

by paleotopography along the northeast-trending structural 

fabric of the raised shoulder of the Reelfoot rift (Palmer, 

1989; He and others, 1997; Seeger and Palmer, 1998). This 

produced a complicated pattern of Late Cambrian sediment distribution varying from (1) very deep depositional 

basin facies centered over the floor of the Reelfoot rift, to 

(2) carbonate shelf facies along the uplifted rift shoulder and 

in the vicinity of paleotopographic Mesoproterozoic basement 

highs, and (3) relatively shallow intrashelf basin facies in 

more foreland areas (Seeger and Palmer, 1998). In the map 

area, the transition from intrashelf facies, called the central 

Missouri basin by Seeger and Palmer (1998), to rift-shoulder 

carbonates is present in the Davis Formation across the 

Wilderness-Handy fault zone (see Lowell and others, 2010). 

Paleotopographic variations along the uplifted rift shoulder, 

from narrow and discontinuous to wide and continuous, also 

contributed to variations in sediment type in the adjacent 

intrashelf basins, from limestone dominated (typical of the 

Bonneterre Formation) to shale dominated (typical of the 

Davis Formation), respectively (Seeger and Palmer, 1998).

Although it failed along the Reelfoot rift, continental 

separation succeeded in opening a major continent-splitting 

ocean basin off the southern margin of the North American 

craton (Laurentia), approximately 200 km to the south of the 

map area. Sedimentation in the tectonically quiescent central 

Missouri basin and Reelfoot rift for the most part infilled and 

smoothed out the paleotopography, except where directly 

adjacent to steep-sided basement highs, which persisted 

as islands. 

For the remainder of recorded geologic time in the 

map area, represented by the uppermost Cambrian and the 

Ordovician section, continental-shelf carbonate deposition 

persisted on the trailing edge of Laurentia. During this time, 

conditions including increasing eustatic levels, increasing 

distance from major terrestrial sediment sources located far to 

the north on the Canadian Shield, and a tropical to subtropical 

latitudinal position, all were conducive to deposition of 

relatively shallow-water carbonate sediments (Repetski and 

others, 1998). Dolomite, formed by both primary-diagenetic 

and secondary-alteration processes, is the dominant lithology 

in the uppermost Cambrian and Lower Ordovician interval 
6 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

(Potosi Dolomite, Eminence Dolomite, Gasconade Dolomite, 

Roubidoux Formation, Jefferson City Dolomite, and Cotter 

Dolomite) (Repetski and others, 1998). Varying mixtures of 

medium- to thin-bedded sandstones are intercalated within 

the Paleozoic section in and above the uppermost Eminence 

Dolomite (see Description of Map Units and Lowell and 

others (2010)).

Rocks exposed in the field area have been near 

the Earth’s surface since at least Mesozoic time, and an 

undetermined amount of erosion has taken place. The color 

alteration index (CAI) of conodonts reported from the Lower 

Ordovician rocks of the southern Ozarks of Missouri is 

1 to 1.5, indicating only low levels of long-term post-burial 

heating that range from ˂ 50 to about 90 degrees Celsius (°C; 

Repetski and others, 1998; Lowell and others, 2010). Based 

on an average geothermal gradient, this suggests that the total 

burial thickness of sediments lying over these conodonts 

has never exceeded about 5,000 to 9,000 ft (1,500 –2,700 m) 

(Epstein and others, 1977).

At several upland locations in the field area, localized 

occurrences of insoluble residuum of Mississippian-age rocks 

indicate that late Paleozoic marine strata once covered the 

region. None of the material at these locations is in place. 

Residuum consists of jumbled chert blocks that are scattered 

across the crests and slopes of hills, indicative of let-down 

residual blocks. The strewn chert fields do not consistently lie 

upon the highest hills in a given area, and their distribution 

in ellipsoidal patches that vary from a few tens of meters to a 

few hundred meters across suggests deposition in paleosinkholes (Bridge, 1930). Collected fossils consist of bryozoan 

fragments and crinoid columnals. More rarely, brachiopod 

molds were recovered, and one mold of a trilobite was 

found in the Birch Tree quadrangle. The brachiopod material 

was sent to Dr. John Carter (Carnegie Museum of Natural 

History, Pittsburgh) and the trilobite specimen was sent to 

Dr. David Brezinski (Maryland Geological Survey, Baltimore) 

for identification; their faunal identifications are presented in 

table 2. 

Table 2. Biostratigraphic determinations for Mississippian chert collections from the Current River drainage basin, Missouri.

[Analyses conducted in 1998 by Dr. John Carter, Carnegie Museum of Natural History, Pittsburgh, and by Dr. David Brezinski, Maryland Geological 

Survey, Baltimore]

Taxon Locality1 Probable source unit or age

Brachiopoda

Avonia minnewankensis or A. williamsana B, BT, W Burlington or Keokuk Limestones

Avonia sp. E Osagean

Brachythris sp. B, BT, W Not age diagnostic

Cyrtina sp.? E Burlington Limestone

Cleiothyridina sp. (large species) B, BT, W Osagean

Eumetria sp. E Burlington Limestone

Echinoconchus alternatus B, BT, W Keokuk Limestone

Girtyella sp. E Not age diagnostic

Punctospirifer sp. (narrow species) E Not age diagnostic

Punctospirifer sp. B, BT, W, E Mississippian

Pustula sp. B, BT, W Burlington Limestone

Rhynchopora sp. B, BT, W Carboniferous or Permian

Schellwienella sp. (large species) E Burlington Limestone

Setigerites setigerus B, BT, W Keokuk Limestone or younger

Spirifer cf. S. grimesi or S. logani B, BT, W Osagean

Tomiproductus sp. B, BT, W Keokuk Limestone

Torynifer sp. B, BT, W Burlington or Keokuk Limestones

Arthropoda

Breviphillipsia semiteretis BT Chouteau Limestone-Reeds Spring FormationPierson Limestone

1

B, Bartlett quadrangle; BT, Birch Tree quadrangle; E, Exchange quadrangle; W, Winona quadrangle. Where B, BT, and W are listed together, the 

collections have not yet been reported separately by locality. 
Discussion 7

Based on faunal collections of chert residuum, at 

least two distinctly different ages appear to be represented. 

The older fauna is indicated by the single trilobite mold of 

Breviphillipsia semiteretis Hessler (1963). Based on the 

Mississippian stratigraphic nomenclature of Weller and 

others (1948), Hessler (1963, 1965) described this fauna as 

occurring in the late Kinderhookian Chouteau Limestone, 

the early Osagean Reeds Springs Formation, the middle 

Osagean St. Joe Limestone Member of the Boone Formation, 

and the middle Osagean Burlington Limestone. This fauna 

also occurs in the Nunn Member of the early Osagean Lake 

Valley Limestone of New Mexico. Brezinski’s (2000) study 

of the Lake Valley Limestone of New Mexico, now known to 

range from Osagean to earliest Meramecian age, shows that 

Breviphillipsia semiteretis occurs in three of the six named 

members: the basal Andrecito and the successive Alamogordo 

and Nunn Members. These three members range from early to 

middle Osagean in age.

Because none of the brachiopod specimens suggest the 

presence of any rocks older than Osagean, and because most 

Kinderhookian-age units have little chert, it seems most likely 

that the trilobite-bearing chert came from either the Pierson 

Limestone or the Reeds Spring Formation of early Osagean 

age or their equivalents. This age is compatible with the 

brachiopod-bearing blocks from the Exchange quadrangle 

that yield large species of Schellwienella and Eumetria, 

Punctospirifer, and Cyrtina? This assemblage is typical of the 

Burlington Limestone (Osagean), which is time equivalent to 

the Pierson Limestone and Reeds Spring Formation but not to 

the overlying Keokuk Limestone (see Thompson, 1986). 

The younger faunal horizon is indicated by brachiopods 

that are characteristic of the Keokuk Limestone or higher 

strata in the region.Setigerites setigerus occurs no lower 

than the Keokuk, Tomiproductus does not occur below the 

Keokuk except in the Cordilleran region, and Echinoconchus 

alternatus is most likely from the Keokuk. Therefore, at 

least two chert-rich Osagean formations were once present 

across the central Salem Plateau but have since been stripped 

away except for remnant residual cherts. None of the fossils 

collected suggests the former presence of any units other than 

ones of Osagean age. 

Surficial Geology

Surficial deposits in the field area include alluvium, 

terrace deposits, residuum, colluvium, and minor loess. 

Overall, surficial deposits are estimated to cover more than 

95 percent of the drainage basins; residuum is the greatest 

surficial deposit volumetrically, and in many areas is more 

than 100 ft (30 m) thick. Surficial deposits are not shown on 

the 1:100,000-scale geologic map but are depicted on the 

1:24,000-scale geologic maps produced for this study (see 

table 1).

Karst Geology

The southeastern margin of the Ozark Plateaus that 

includes the map area is one of the most karstified regions 

in the United States. Karst development is characterized by 

well-developed and integrated underground drainage systems, 

long segments of losing and disappearing streams, long 

segments of gaining streams, hundreds of caves, thousands 

of sinkholes, and dozens of major springs, some of which are 

world class. The three major waterways in the study area, the 

Current River, its tributary the Jacks Fork, and the Eleven 

Point River (fig. 2A), are renowned for having the highest 

number of first-order-magnitude springs in the United States. 

Hundreds of second- and third-order-magnitude springs also 

occur along the rivers and their minor tributaries. There is 

strong correlation between the flow magnitudes of springs in 

the Current and Eleven Point River basins and the lengths of 

the interconnected cave networks that serve as groundwater 

conduits. Detailed discussions of Big, Round, and Alley 

Springs can be found in Lowell and others (2010).

A better understanding of the hydrogeology of the karst 

system is gained by groundwater dye-trace studies, which 

help define subsurface recharge areas (subsurface drainage 

basins) for spring discharge; however, such studies are 

limited as they are incapable of revealing actual flow paths. 

Dye-trace studies for major springs in the map area (Aley 

and Aley, 1987; Imes and Kleeschulte, 1995) show crossing 

trace paths, long distance of travel, overlapping subsurface 

drainages, and nonequivalent surface and subsurface drainage 

basins. Additional complexity in the hydrologic system also is 

revealed by the highly irregular regional groundwater surface 

and the distribution of losing and gaining streams (Gann and 

others, 1976). 

Despite this complexity, our fieldwork recognized some 

of the major geologic controls on the development of karst 

features, particularly caves and springs, that are of both 

primary and secondary origin. Primary geologic controls that 

influence water flow and rock dissolution for cave or conduit 

formation include sedimentary features inherent from deposition and diagenesis; the major controlling features include 

bedding-plane partings, vertical variations of depositional 

facies within the Paleozoic section, and topographic relief 

on the unconformity between the basement (confining unit) 

and the overlying Paleozoic section. Virtually all caves are 

developed parallel or subparallel to bedding planes, and their 

vertical advances are almost strictly the result of physical 

stoping. Cave mapping for this project in the Current and 

Eleven Point River basins further identified an overall branchwork morphology of cave passages, similar to that identified 

by Dom and Wicks (2003) for approximately 72 percent of 

all caves in the Salem Plateau. Palmer (1991) showed that 

branching cave systems are indicative of bedding control, 

whereas curvilinear passages of branchwork morphology are 

controlled by bedding-plane-parting porosity. The Ozark caves 
8 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

are known to be concentrated at several discrete stratigraphic 

horizons:one level in the upper part of the Eminence Dolomite 

and one in the upper part of the Gasconade Dolomite.

Secondary geologic controls are largely restricted to 

dissolution-enhancing ground preparation created by fault 

movement in the Paleozoic section. This is particularly true 

for paleo-karst associated with the Wilderness-Handy fault 

zone (see Lowell and others, 2010, Stop 11 discussion). In 

rocks exposed at the surface, mostly the Eminence Dolomite 

and overlying section, jointing appears to play a subordinate 

role in karst development. This is probably because joints in 

the Current and Eleven Point River basins typically are not 

throughgoing, instead breaking only a single or at the most 

a few bedding horizons, and thus not developing vertically 

connected conduits capable of significant water flow. The joint 

fabric in the Derby-Doerun Dolomite and older rocks is not 

known, largely due to their subsurface occurrence. The joint 

fabric in the overlying Potosi Dolomite is only poorly known.

Progressive downcutting by the larger surface streams in 

the study area has lowered the elevation of the water table and 

stranded many caves, especially in the Current River basin, at 

levels well above the present groundwater surface. Some of 

these caves have immense rooms and channels indicative of 

large volumes of water flow. These stranded caves are comparable in scale to known present-day spring conduits such as 

Alley Spring (see Lowell and others, 2010), and they serve 

as ancient analogues to the conduits that exist in the shallow 

subsurface of the Ozarks today. 

More than 700 caves are known in the field area, of 

which 79 were studied to gain understanding of the geologic 

controls on the development of groundwater conduits along 

the southeastern margin of the Ozark Plateaus. Geologic 

mapping of 19 of these caves collected information on the 

stratigraphy, passage orientations, fractures, and passage 

morphology (Šebela and others, 1999; Orndorff and others, 

2001). In addition, maps of 60 other caves, produced by the 

Cave Research Foundation, were examined for information 

on passage orientation and morphology (for example, see 

Missouri Speleological Survey, 1977, 1982a,b, 1984).

Sinkholes

Combining geologic mapping and geographic information

system (GIS) analysis, Orndorff and others (2000) concluded 

that several geologic, physiographic, and hydrogeologic 

parameters are related to sinkhole development. Most of the 

sinkholes in the study area occur in the Roubidoux Formation 

and Jefferson City Dolomite, the two formations of the 

Paleozoic section that contain more numerous sandstone beds 

and that have the greatest aerial extent in the mapped area. 

Regionally, these two units also form the upper surfaces of 

high plateaus.

Weary and Orndorff (2001) discussed how simple 

stratigraphic analysis of sinkhole occurrence can be 

misleading. For example, sinkholes shown on geologic maps 

as occurring in the Roubidoux Formation actually develop by 

collapse or subsidence into dissolution voids in the uppermost 

part of the Gasconade Dolomite. Therefore, the morphology 

of sinkholes is related to dissolution of dolostone directly 

beneath the sandstone beds (Orndorff and others, 2006). Many 

of the sinkholes observed in the field area are bedrock-collapse 

sinkholes formed by collapse of sandstone beds into large 

dissolution voids in subjacent dolomite beds. These sinkholes 

are characterized by very steep to vertical sides and are 

commonly rimmed by intact sandstone beds or slabby sandstone float blocks. This is in contrast to most karst areas and 

sinkhole plains, where cover-collapse sinkholes (sinkholes in 

the soil mantle characterized by more gentle slopes and rarely 

involving bedrock collapse) predominate. Sinkholes in the 

study area that are located away from the major river valleys 

in upland areas of the Salem Plateau, as well as sinkholes 

elsewhere in Missouri, tend to be of the cover-collapse type 

due to the thick residuum and soil overlying the bedrock.

Structural Geology

Sedimentary strata in the map area are generally 

subhorizontal to gently dipping, with gentle, open folds 

developed in compressional (or transpressional) domains 

near faults and in subsidence features related to large karstic 

voids. For most of the area, bedding dips of less than 2° are 

predominant, with the regional directional trend toward the 

south. Small, subtle folds, both anticlines and synclines, were 

observed at various locations in the map area, particularly 

along reaches of the larger rivers where continuous rock 

exposure occurs. These folds were generally too small to 

portray at map scale. A few larger folds, apparent via map 

pattern, are indicated by symbols on the map. 

At many localities Paleozoic strata locally dip radially 

away from topographic highs on the Mesoproterozoic rock 

surface as a result of differential compaction and (or) nonhorizontal primary deposition. Dip angles as steep as 38° have 

been reported in these strata within the study area (Harrison 

and others, 2002).

Similar to Mesoproterozoic rocks in the St. Francois 

Mountains, basement rocks in the map area also lack any 

penetrative structural fabric, indicating that these rocks have 

never been buried more than a few kilometers (Kisvarsanyi, 

1981). In the field area, the observed and inferred fault pattern

developed in Paleozoic rocks is similar to that found in basement 

rocks, leading to the conclusion that the Proterozoic basement 

fabric exerted a controlling influence on younger Paleozoic 

structures. Regionally there are two dominant fault trends, one 

oriented northeast and the other oriented northwest. Lesser 

north-trending and east-trending faults have been mapped 

locally. Similar trends in regional strike patterns are described 

elsewhere in southeastern Missouri (McCracken, 1971; Harrison 

and Schultz, 2002). This northeast-northwest bimodal structural 

trend is widely thought to be inherent from structures in the 

Proterozoic basement rocks (McCracken, 1971; Kisvarsanyi, 

1974; Kisvarsanyi and Kisvarsanyi, 1976; Clendenin and others, 

1989, 1993; Lowell, 2000; Harrison and Schultz, 2002). 
Discussion 9

On the basis of tectonically disturbed stata, three broad 

age groups of faults are discernible: (1) those showing 

evidence that they were active only in the Mesoproterozoic, 

(2) those that were active at one or more times prior to 

deposition of the Ordovician section (that is, Neoproterozoic 

through Late Cambrian), and (3) those that were active at one 

or more times in the Phanerozoic and probably during the 

Proterozoic. From field relations observed in the map area, we 

can determine that the youngest faulting is post-Ordovician 

in age. Faults of age group 3, in part, are likely associated 

with the late Paleozoic ancestral Rocky Mountain-OuachitaAlleghenian orogenic systems, as the Ouachita front is only 

about 200 km to the south; see Cox (2009) and Hudson (2000) 

for analyses of late Paleozoic faulting in the Ozark region. 

Tectonic features (Craig and Connor, 1979) show that uplift 

in northwestern and central Missouri had begun in the Late 

Mississippian, producing an elongated northwest-trending 

ridge that projects through the map area along the central 

Missouri tectonic zone of Kisvarsanyi (1981, 1984) (see 

figure 3 and cross sections). By Early Pennsylvanian time, this 

elongated uplift, known as the Pascola arch, had grown to the 

southeast and extended to the Reelfoot rift and beyond to the 

Nashville dome (Grohskopf, 1955). The crest of the Pascola 

arch had as much as 7,900 ft (2,400 m) of uplift (Marcher and 

Stearns, 1962) where it crossed the Reelfoot rift, effectively 

cutting off sediment flow out the southern end of the Illinois 

basin (Kolata and Nelson, 1990).

Northeast-Trending Faults

The Wilderness-Handy fault zone is the longest, most 

continuous northeast-trending structure in the map area 

and appears to exert significant influence on groundwater 

flow (see Hydrogeology section below and Lowell and 

others (2010)). This fault zone, only a few kilometers in 

width, consists of parallel to braided fault strands that have 

been mapped at 1:24,000 scale between the Current River 

at Van Buren, Mo., and Horseshoe Bend on the Eleven 

Point River near Greer, Mo. (fig. 2B). The fault zone is 

inferred to extend on strike from the Eleven Point River to 

Thayer, Mo. (fig. 2B), where a northeast-trending fault zone 

mapped by Hedden (1968) is interpreted as its continuation. 

Reconnaissance mapping between the Eleven Point River and 

Thayer found a paucity of outcrops and no reliable structural 

data, and little subsurface drill-hole data available for this area.

Drill-hole data available from a segment of the fault zone 

near Van Buren indicate that the Cambrian section within 

the Wilderness-Handy fault zone is more intensely faulted 

than the exposed Ordovician section (for details see Harrison 

and McDowell, 2003; Lowell and others, 2010). In both the 

Thayer and Van Buren areas, where exposures are relatively 

good and detailed mapping exists, northeast-striking faults 

of the Wilderness-Handy fault zone appear to cut northwesttrending faults, suggesting that northeast-trending faults 

have experienced more recent movement. This is contrary to 

the relationship shown by Clendenin and others (1989) that 

showed the northwest-striking faults cutting those with a northeast trend. The Wilderness-Handy fault zone is assumed to cut 

the northwest-trending Teresita fault, but poor exposures in the 

intersectional area prevent us from having actual evidence.

In addition to the Wilderness-Handy fault zone, numerous 

other northeast-trending faults are portrayed on the geologic 

map. In the southern one-third of the map area, faults of this 

trend are thought to occur in areas of very poor to nonexistent 

bedrock exposure on the upland plateau area where, except 

for the Grand Gulf fault, they are inferred from drill-hole and 

aeromagnetic data. The Grand Gulf fault is exposed in walls 

of a collapsed cave system at Grand Gulf State Park, about 

10 km west-northwest of Thayer. Extension of this fault along 

strike from this locality is tentative. In the northeast-central 

region of the map area, several northeast-trending faults were 

identified near the cluster of exposed Mesoproterozoic basement protrusions. Detailed 7.5-minute quadrangle mapping 

around the basement protrusions shows that these faults 

have offset the Mesoproterozoic rocks much more than the 

Paleozoic stratigraphy (Orndorff and others, 1999; McDowell 

and Harrison, 2000; Harrison and others, 2002). Several of 

these structures are associated with linear magnetic anomalies 

interpreted as Mesoproterozoic shear zones (Harrison and 

others, 2002). Kinematic indicators associated with two 

of these northeast-striking shear zones, Denning Hollow 

and Mud Spring Hollow, suggest that left-lateral strike-slip 

faulting during the Proterozoic (Harrison and others, 2002) 

was followed by re-activation at undetermined times. 

Northwest-Trending Faults

The dominant trend of faults in the field area, both 

mapped and inferred, is northwesterly. A structural crosssectional transect (A–A') from the southwest-central part of 

the map area to the northeast corner encounters at least three 

zones of faulting (fig. 3): (1) the central Missouri tectonic 

zone of Kisvarsanyi (1984), considered by her as a crustalscale zone of deformation in the basement fabric; (2) faults 

related to the Eminence caldera discussed previously; and 

(3) the Ellington fault zone, which is interpreted by Clendenin 

and others (1989) as a long-lived zone of crustal-scale 

deformation. These faults are likely related to the BolivarMansfield fault system, which McCracken (1971) envisioned 

as extending across the entire southwest corner of Missouri 

from the Kansas border into Arkansas. All of these structures 

are thought to continue southeastward to and beneath the 

Mississippi embayment. 

The Alice Mine fault is tentatively mapped along a 

prominent magnetic linear anomaly trending about N. 60o W. 

in the extreme southwest corner of the map area. From 

exposures located a few kilometers to the west of the map 

area, the Alice Mine fault is described by Kidwell (1946) as an 

elongated collapse structure striking approximately N. 70o W. 

to N. 80o W. that has about 18 ft (5.5 m) of down-to-the south 

displacement. McCracken (1971) suggests that this structure is 

a highly brecciated strike-slip fault.
10 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

The West Plains-Thayer fault zone, which represents the 

southeastward continuation of the Bolivar-Mansfield fault 

system, is relatively well-exposed to the west of the map 

area, where it deforms rocks as young as Pennsylvanian (see 

McCracken, 1971; Middendorf and others, 1991). In the West 

Plains area (fig. 2B), the existence of the West Plains-Thayer 

fault zone is based on differences in elevations of stratigraphic 

contacts in drill holes (see Missouri Department of Resources 

(2012) online well database at http://www.dnr.mo.gov/env/wrc/

logmain/index.html) and the trace is considered approximately 

located. The West Plains-Thayer fault zone is better exposed 

in the Thayer area, where it was mapped by Hedden (1968). 

Northwest of the Thayer area, this fault zone is portrayed as a 

single strand, although it likely comprises multiple complex, 

braided to en echelon fault strands that are similar to those 

mapped in the Thayer area and along the Bolivar-Mansfield 

fault system (Middendorf and others, 1991). 

The central Missouri tectonic zone of Kisvarsanyi (1981, 

1984) extends from the Midcontinent Rift system in Nebraska 

to the Mississippi embayment in southeastern Missouri. 

This tectonic zone is associated spatially with a geophysical 

anomaly called the Missouri gravity low (see Lowell and 

others (2010) and Harrison and Schultz (2002) for discussions 

on the Missouri gravity low). The central Missouri tectonic 

zone traverses the entire map area from northwest to southeast 

and is represented on the magnetic survey map (fig. 3) as a 

belt having an overall magnetic-low signature and bounding 

linear anomalies. Two northwest-striking faults, the Teresita 

and Houston faults, which cut the Paleozoic section, are 

thought to represent re-activation of basement structures along 

the central Missouri tectonic zone. 

The Teresita fault appears to be a continuous structure 

across the entire map area and is spatially associated with a 

linear trough in the regional groundwater surface (see text 

below and Lowell and others (2010) for further discussion). 

The portrayal of the Teresita fault in the southeast corner 

of the field area is based on unpublished geologic mapping 

in files of the Missouri Geological Survey in Rolla. In the 

western part of the map area the location of the Teresita fault 

is constrained by drill-hole data and the fault is considered 

approximately located. On cross sections A–A' and B–B' the 

Teresita fault is interpreted as the southwestern boundary 

of the central Missouri tectonic zone. The fault appears to 

scissor along strike, so that along its eastern extent (east of 

the trace of cross section A–A') strata are downthrown to the 

southwest, while along its western extent strata are downthrown commonly to the northeast. In the south-central part 

of the study area, where the Teresita fault crosses the Eleven 

Point River, stratigraphic offset of the Gasconade DolomiteRoubidoux Formation contact across the fault is minor (Weary, 

2008b). A down-to-the northeast, northwest-trending fault has 

been mapped on-strike with the Teresita fault in the adjacent 

Springfield 1°×2° quadrangle to the west of the map area 

(Middendorf and others, 1991). Because of its long strike 

length, relatively minor vertical offset, and scissoring nature, 

the Teresita fault is interpreted to be a strike-slip structure.

The Houston fault disrupts bedding within the Gasconade 

Dolomite in a roadcut along U.S. Route 63 at the northern 

outskirts of Houston, Mo., near the northwestern corner of the 

study area (fig. 2B). From here, along strike to the northwest 

in the map area, the Houston fault is a down-to-the southwest 

structure that juxtaposes Gasconade Dolomite against the 

Roubidoux Formation. Still farther to the northwest, a 

down-to-the-southwest fault mapped by Middendorf and 

others (1991) in the adjacent Springfield 1°×2° quadrangle is 

considered to be a continuation of the Houston fault. Southeast 

of the town of Houston, the Houston fault is approximately 

located based on subsurface drill-hole data, as well as on both 

reconnaissance and detailed mapping, for a distance of about 

66 km before it either dies out within the Ordovician section 

or its stratigraphic offset is so minor that it becomes untraceable at the surface. The geophysical survey conducted by 

Spector (1982) indicates that the Houston fault trend continues 

southeastward in the Mesoproterozoic basement to as far as 

the Wilderness-Handy fault. Spector’s (1982) data also suggest 

that after a right-lateral offset across the Wilderness-Handy 

fault, the Houston fault trend in the Mesoproterozoic basement 

continues yet farther to the southeast. 

The Houston fault marks the northeastern boundary 

of the central Missouri tectonic zone, as it is the apparent 

boundary between differing Mesoproterozoic units (such as 

Y2g and Y1g on cross section A–A', and Y1v and Y1g on cross 

section B–B'). The Precambrian basement map of Sims (1990) 

suggests between 30 and 100 km of left-lateral offset of the 

contact between Paleoproterozoic metamorphic rocks and 

Mesoproterozoic igneous rocks across the central Missouri 

tectonic zone (see figure 8.7 of Lowell and others, 2010). 

Drill-hole and aeromagnetic data suggest a possible 20 km of 

left-lateral offset of Mesoproterozoic volcanic rocks across the 

Houston fault in the subsurface of the central part of the map area.

In the upper part of the Jacks Fork drainage, three 

relatively short north- to northwest-trending faults (the Fly 

Blow Hollow, Buck Hollow, and Belew Hollow faults) have 

been mapped between the Teresita and Houston faults. These 

three faults merge toward the southeast where they either 

terminate within the Ordovician section or the observed 

stratigraphic offset becomes insufficient to map. A prominent 

linear magnetic anomaly (fig. 3) projects several kilometers 

farther to the southeast from the fault terminations, suggesting 

that the faulting may continue in the Mesoproterozoic basement in that direction. This projection also coincides with 

a linear stretch of the South Fork of Hurricane Creek, and 

main stem Hurricane Creek drainages, suggesting a possible 

structural control.

With orientations that are parallel to or en echelon with 

the structural trend of the Houston fault is a discontinuous 

linear series of individual faults called, from northwest to 

southeast, the Low Wassie, Evans Hollow, and Eastwood 

faults. This structural trend is cut by at least four northeasttrending strands of the Wilderness-Handy fault zone (see 

7.5-minute geologic maps for more details on these faults). 

The structural trend was interpreted as a regional strike-slip 
Discussion 11

fault by Clendenin and others (1989), who referred to it as 

the Shannon County fault. Horizontal slickenside striations 

observed in drill-hole samples of the Cambrian part of the 

section along the Low Wassie fault provide further evidence 

of Paleozoic strike-slip movement for this structure (Orndorff 

and Harrison, 2001).

In the northwest corner of the study area our Hartshorn and 

Sutton Creek-Ink faults were originally mapped in reconnaissance by Satterfield (1976) and called, respectively, the Arthur 

Creek and Oscars faults. The Big Creek fault was identified 

during our detailed mapping in the Montauk quadrangle. 

Westward continuations of the Hartshorn and Sutton Creek-Ink 

faults have been mapped on the adjacent Springfield 1o×2o 

quadrangle (Middendorf and others, 1991). Our mapping has 

extended the Hartshorn and Sutton Creek-Ink faults eastward 

into the western part of the Eminence caldera (fig. 3). Both of 

these faults display reversals in stratigraphic offset, or scissoring, suggesting a strike-slip component to their movement.

The Gladden Creek fault was mapped in the Cedargrove 

quadrangle in the north-central part of the map area (Weary, 

2008a). The fault extends to the northwest into the adjacent 

Montauk quadrangle where identifiable offset along it diminishes, making it unmappable (D.J. Weary, USGS, unpub. data, 

2013). The Gladden Creek fault is inferred to extend to the 

southeast from the Cedargrove quadrangle into the northern 

part of the Eminence caldera, based on drill-hole and aeromagnetic data (fig. 3). The fault displays scissoring, suggesting 

that it is a strike-slip fault.

The Ellington fault zone is a strike-slip system that 

exhibits left-lateral movement (Clendenin and others, 

1989; Taylor, 1983). This fault zone is well known from 

underground exposures in the Sweetwater Mine (see below 

for discussion) and from drilling in the vicinity of Ellington, 

Mo. (fig. 2B) (McCracken, 1971). Reconnaissance mapping 

of this study extends the Ellington fault zone beyond the 

northern edge of the map area (see Stop 3 in Lowell and 

others, 2010). Within the Sweetwater Mine orebody, parts 

of the Ellington fault zone are mineralized. This relationship 

aided Clendenin and Duane (1990) in their interpretation that 

northwest-trending fault zones in southeastern and southern 

Missouri (including the Ellington and Low Wassie-Evans 

Hollow-Eastwood faults) provided pathways for mineralizing 

Mississippi Valley-type base-metal fluids.

The Bunker fault, located in the northeastern part of 

the map area, is inferred both from drill-hole data and from 

a prominent linear magnetic anomaly (fig. 3). Drill holes 

located in and around the town of Bunker (fig. 2B) indicate 

that the Bunker fault is a down-to-the-northeast structure that 

juxtaposes the Roubidoux Formation against the Gasconade 

Dolomite. The Bunker fault, as inferred from the aeromagnetic 

data, is a linear anomaly that appears to merge with the 

Ellington fault zone near the eastern edge of the map area.

The Webb Creek fault is a northwest-striking structure 

near the eastern edge of the study area that is inferred from 

drill-hole data. These data indicate an area of uplift exists 

between the Webb Creek fault and the Ellington fault zone; 

an anomalous outcrop of Mesoproterozoic granite (unit Y1g) 

located between these two faults also implies structural uplift. 

The north-trending Pine Valley Creek fault, inferred from 

anomalies in the aeromagnetic data, provides a structural link 

between the Webb Creek fault and the Ellington fault zone 

and forms the western side of the uplift. The uplift area is 

rhomb-shaped if the eastern edge of the map area is considered 

its eastern side. A possible explanation for the uplifted area 

is that it is in a restraining bend created by a right step in the 

left-lateral Ellington fault zone.

A small segment of the Black fault, located in the 

northeast corner of the map area, was delineated in reconnaissance mapping by Middendorf in the Centerville quadrangle 

(1979). This fault bounds the southern edge of the St. Francois 

igneous terrrane (Clendenin and others, 1989) and is believed 

to be a strike-slip structure that exhibits a left-lateral sense of 

motion. Rocks to the north of the fault exhibit upward vertical 

offset relative to rocks to the south.

Seismicity

Seismicity in the map area has been sporadic, relatively 

widespread, historically of low magnitudes (Hadley and 

Devine, 1974; Nuttli and Brill, 1981; Dewey and others, 

1989), and typically only locally felt. Recorded epicenters 

from the most recent earthquakes, for the years 1964 through 

2003, are plotted on the geologic map (Missouri data may 

be accessed via search tools at the USGS Earthquake 

Hazards Program online databases, http://earthquake.usgs.

gov/earthquakes/states/?region=Missouri; and also at the 

University of Memphis, Center for Earthquake Research 

and Information, http://www.ceri.memphis.edu/seismic/). 

Magnitudes of these earthquakes range from 2.5 to 5.1 on the 

Richter scale and reported depth ranges are shallow (0–12 km 

below the surface). 

The few focal-mechanism solutions that have been 

obtained for earthquake events near the study area indicate 

that the regional compressional stress field in the central 

United States is oriented east-northeast (Zoback and Zoback, 

1991; Zoback, 1992). Hermann and Nguyen (1992) corrected 

and verified previously published focal mechanism solutions 

using waveform modeling of broadband data in complement 

with regional seismic-network data.

Mississippi Valley-Type Base-Metal Occurrences

The two southernmost active mines in the Viburnum 

Trend exploiting Mississippi Valley-type (MVT) base-metal 

mineralization are the Fletcher Mine and the Sweetwater 

Mine, both located within the map area (fig. 2A). These mines 

are currently owned and operated by the Doe Run Co. Both 

operations are located in the upper Black River drainage basin; 

however, the underground workings of the Sweetwater Mine 

are located within the subsurface recharge area for springs 

that feed the Current River (Feder and Barks, 1972; Maxwell, 

1974; Aley and Aley, 1987).
12 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Fletcher Mine

The discovery hole for the Fletcher Mine, located in 

sec. 13, T. 32 N., R. 2 W., was drilled in 1958; shaft excavation began in 1964, and milling operations began in early 

1967 (Paarlberg and Evans, 1975). Ore principally occurs as 

disseminations and stratabound bands in beds of laminated 

siltstone and oolitic grainstone, the latter having algal 

characteristics, within the upper Bonneterre Formation, but 

some ore also occurs in brecciated parts of the overlying Davis 

Formation of the Elvins Group (Paarlberg and Evans, 1977). 

Two ore bodies are mined at Fletcher: one that is draped over 

the axis of a north-trending Precambrian basement protrusion, 

and another that occurs directly over a pinchout of the Lamotte 

Sandstone on the west flank of the same protrusion (Paarlberg 

and Evans, 1975, 1977). 

Sweetwater Mine

The Sweetwater Mine (see cross section A–A′) is the 

southernmost mine in the Viburnum Trend; it has also been 

known as the Ozark Lead mine, the Frank R. Milliken Mine, 

and the Adair Creek Mine (it is labeled Adair Creek Mine 

on the geologic map). The occurrence of MVT economic 

mineralization at this location was discovered in 1962 and 

mine production commenced in 1968 (Mouat and Clendenin, 

1975). The orebody consists of several ore shoots that occur 

throughout the Bonneterre Formation comprising multiple 

stratabound horizons of dominantly digitate algal boundstones 

and oolitic grainstones, and is in proximity to a series of northwest-trending basement protrusions (Mouat and Clendenin, 

1975, 1977). Two differing deformational processes contributed to ground preparation for mineralization: (1) multiple 

complex episodes of sediment gravity-sliding away from 

the basement protrusions, with associated solution collapse 

(Larsen and others, 1979) and (2) transtensional dilation in 

a left-lateral shear couple (Taylor, 1983). Given the similar 

timing with deformation in the nearby Reelfoot rift, the gravity 

slides could well have been seismic in origin.

The Sweetwater ore deposit overlies the location of 

local basement protrusions that are situated primarily on 

the upthrown side of a high-angle reverse-fault strand of 

the northwest-trending Ellington fault zone (Mouat and 

Clendenin, 1977; Paarlberg and Evans, 1977). As discussed 

previously, the Ellington fault zone is a left-lateral, strikeslip system. Because parts of the Ellington fault zone are 

mineralized within the orebody, Clendenin and Duane 

(1990) concluded that northwest-trending fault zones in 

southeastern and southern Missouri provided pathways for 

mineralizing MVT fluids. The Sweetwater and Suses Branch 

faults, both major strands of the Ellington fault zone, partition the Sweetwater deposit into three orebodies (B. Walker, 

Sweetwater Mine geologist, oral commun., 1996). Base-metal 

mineralization between the Sweetwater and Suses Branch 

faults occurs in northeast-trending en echelon ore shoots 

(Taylor, 1983), a geometry that is consistent with right-lateral 

horizontal strain along a conjugate Reidel shear related to the 

left-lateral motion of the Ellington fault zone (see schematic 

plan view above the Ellington fault zone on cross section 

A–A′). In workings of the Sweetwater Mine, exposures of the 

Ellington fault zone exhibit multiple episodes of pre- and postore emplacement strike-slip faulting (Taylor, 1983; Clendenin 

and others, 1989).

Within the Sweetwater Mine, the Sweetwater fault acts 

as an aquitard (B. Walker, Sweetwater Mine geologist, oral 

commun., 1996). Vertical movement has offset the Davis 

Formation-Bonneterre Formation contact by approximately 

100 ft (30 m) across the fault. Dewatering of the uppermost 

bed of the Bonneterre Formation in the hanging wall produced 

no change in hydrologic conditions in the uppermost bed 

of the Bonneterre Formation in the footwall, nor do mine 

workings “make water” (release excess water) from the fault 

zone itself when they crosscut it (B. Walker, Sweetwater Mine 

geologist, oral commun., 1996).

Mississippi Valley-type base-metal deposits are known 

to occur beneath the drainage basin of Blair Creek (see 

cross section A–A′), which is a tributary of the Current River 

(Kisvarsanyi, 1977). These occurrences were drilled in the 

1960s and the results are proprietary.

In an area located several kilometers north of Greer Spring, 

numerous drill holes encountered trace to large amounts of 

base-metal mineralization, principally within the Bonneterre 

Formation. Lesser mineralization was encountered within other 

units. The most significant mineralization found to date occurs 

within the Bonneterre Formation beneath the small drainages 

of Becky Hollow, Mine Hollow, McCormack Hollow, and 

Threemile Hollow in secs. 2, 3, 10, 11, 14, 15, and 22, T. 25 N., 

R. 4 W., in the Greer and Piedmont Hollow 7.5-minute quadrangles. These drainages flow a short distance (3–5 km) into the 

Eleven Point River. Table 3 summarizes the high-grade metal 

occurrences encountered.

Table 3. Summary of high-grade base-metal mineralization 

encountered in drill holes in the Bonneterre Formation several 

kilometers north of Greer Spring, Mo.

[Drill-hole locations are shown on the geologic map within the outlined area 

marked “Area of figures 6 and 7” and are listed in appendix 1]

Drill-hole

number

Thickness

recovered,

in feet

Metal concentration in

recovered interval, in percent

Lead Zinc

801-129 1.0 26.5 1.2

801-148 1.0 11.0 2.9

84W40 6.2 35.9 12.2

86W4 4.0 75.4 25.6

86W6 18.4 66.1 11.2
Discussion 13

Audio-Magnetotelluric (AMT) Survey

In an effort to better understand the anomalous mineral 

occurrences in the area north of Greer Spring, in the vicinity 

of the above-mentioned drill holes, audio-magnetotelluric 

(AMT) soundings were made to determine variations in the 

electrical resistivity of the earth with depth. AMT sounding 

uses natural-source, multi-frequency electromagnetic signals 

from lightning or other atmospheric disturbances as an energy 

source (Cagniard, 1953; Dmitriev and Berdichevsky, 1979; 

Wait, 1962). AMT soundings consist of electric and magnetic 

field measurements taken over a four-decade range of frequencies from 10 to 100,000 Hertz (Hz). The resultant distribution 

of currents induced in the earth is dependent on the electrical 

resistivity and magnetic permeability of the earth and the 

frequency measured. Since low-frequency signals penetrate 

to greater depths than high-frequency signals, measurements 

of the electromagnetic response at several frequencies contain 

information on the variation of resistivity at depth. Data from 

these sounding traverses are inverted and stitched together to 

form depth profiles that are oriented at various angles to the 

buried geologic structures. AMT tensor soundings collected 

by Herbert A. Pierce (USGS) during the spring of 2001 in the 

proposed prospecting-permit-application area (see figure 2A

for location) were recorded using a Geometrics EH-4 system. 

No vertical magnetic field (Hz) data were recorded because 

the system is limited to four channels (Ex, Ey, Hx, and Hy ). 

Initially about 2,000 frequencies were collected and then 

reduced to approximately 40 frequencies (10 per decade) for 

each of the two (X and Y) directions from 10 to 100,000 Hz. 

The magnetic field sensors, electric field sensors, buffers, 

and pre-amplifiers for both systems, including a 60-Hz notch 

filter to reduce interference from electric power lines, were 

manufactured by Electromagnetic Instruments, Inc. (EMI), 

now Schlumberger EMI Technology Center. 

In our AMT survey, the Geometrics EH-4 receiver 

employed a two-stage coefficient-of-coherence cutoff 

filter that first removed any signals having a coefficient of 

coherence less than 0.3, then removed any signals having 

coefficients of coherence less than 0.5 in the second stage. 

Signal amplitudes were monitored, and any that saturated 

the receiver amplifiers were rejected. Time series that had 

more than seven sensor or instrument saturations were also 

rejected. Assessments were made of the sounding locations 

before and after data collection. Sites were chosen so that 

stations were more than 100 m away from power lines. 

Background electric and magnetic fields were monitored prior 

to recordings, and stations were moved if the static fields 

were above 200 millivolts (mV) on the electric lines or above 

150 nanoteslas (nT) on the magnetic coils. Two-dimensional 

invariant inversions of the collected data were completed 

using a uniform half-space starting with 100 ohm-meters. 

They are presented in map form and as electrical sections 

or profiles (figs. 6 and 7, respectively), discussed below. 

Calculated values of phase-sensitive skew indicate that 

two-dimensionality is a good assumption for most frequencies. 

Generally all frequency decades, 100,000 Hz to 10 Hz, have 

skews less than 0.25. 

Inverted data from 24 AMT soundings collected in 

the vicinity of high-grade base-metal mineralization were 

combined into a map (fig. 6) and two vertical depth profiles 

(figs. 7A and B). The map view, which is at an elevation of 

300 m below mean sea level, shows an area of relatively 

low resistivity coincident with four out of the five drill holes 

containing anomalously high values of lead and zinc mineralization (table 3). The low resistivities suggest that the mineralization is related to measurable lower resistivity values. 

Drill holes 801-148, 84W40, 86W4, and 86W6 are within the 

low-resistivity area on the map; although drill hole 801-129 

also has high values of mineralization, it is located outside and 

north of the 2001 AMT survey grid. Figure 7 shows the eastand northeast-oriented two-dimensional electrical profiles. 

The low resistivity values calculated by the finite-difference 

two-dimensional modeling of the electrical soundings are 

shown as blue areas. 

On the east-oriented invariant electric traverse profile 

(fig. 7A) the low-resistivity area outside of the measured 

mineralization appears to extend nearly to the surface, possibly 

indicating alteration and increased permeability related to the 

mineralizing process. The northeast-oriented invariant electric 

traverse profile (fig. 7B) does not have low resistivity values 

that continuously approach the surface. 

The processed AMT data appear to convincingly delineate the volume of lead/zinc mineralization in the area north 

of Greer Spring. Electrical sections and map images of the 

resistivity below and near the area of base-metal mineralization recovered the depths and lateral extent of the known 

mineralized area. The extent of mineralization to the north of 

the main cluster of discovery drill holes, indicated by a single 

drill hole (801-129), was outside the spread of AMT sounding 

sites, so limits to the mineralized body to the north could not 

be estimated. Additional AMT soundings to the north would 

probably better define the extent of this deposit.
14 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Hydrogeology 

Geohydrologic units for the Ozark Plateaus physiographic province, which encompasses the map area, have 

been established as the Ozark Plateaus geohydrologic system 

(Gann and others, 1976; Imes, 1989; Imes and Smith, 1990; 

Imes, 1990a,b; Kleeschulte, 2001). This vast system extends 

throughout southern Missouri, northern Arkansas, and eastern 

parts of Oklahoma and Kansas. The Ozark Plateaus geohydrologic system consists of four major geohydrologic units, 

which in ascending order include the basement confining 

unit, the St. Francois aquifer, the St. Francois confining 

unit, and the Ozark aquifer (see figure 4) (Gann and others, 

1976; Imes, 1989; Imes and Smith, 1990; Imes, 1990a,b; 

Kleeschulte, 2001). The basement confining unit comprises 

the Mesoproterozoic volcanic and plutonic basement rocks 

of the St. Francois terrane and Paleoproterozoic metamorphic 

rocks (Imes, 1989). These dense basement rocks are largely 

highly impermeable, except along faults and fracture zones 

where small water yields are possible (Imes, 1989). The 

St. Francois aquifer comprises Upper Cambrian strata that 

disconformably overlie the basement confining unit and 

conformably underlie the St. Francois confining unit (Imes, 

1990a). In the map area, the St. Francois aquifer consists of 

a basal conglomerate of the Lamotte Sandstone that exists 

on top of the major Proterozoic-Paleozoic unconformity, the 

remainder of the Lamotte Sandstone, and the Bonneterre 

Formation. From drill-hole data, the basal conglomerate of the 

Lamotte appears to be ubiquitous, although it is generally very 

thin (<20 ft) (6 m). The Lamotte Sandstone generally thickens 

toward the west in the study area, although it is known to be 

absent adjacent to or over many basement highs. Bounding 

the top of the St. Francois aquifer is the St. Francois confining 

unit, which is composed of the Cambrian Elvins Group. 

The Elvins Group is subdivided into the Davis Formation 

and overlying Derby-Doerun Dolomite (usage of Missouri 

Geological Survey, 1979). West of the Wilderness-Handy fault 

zone, these stratigraphic units contain beds of shale, shaly 

mudstone, and thinly bedded, dense, fine-grained dolomites, 

which analyses have shown are nonporous (primary porosity) 

and very impermeable (Kleeschulte and Seeger, 2000, 2001). 

No studies have been undertaken to evaluate the secondary 

porosity of these rocks. East of the Wilderness-Handy fault 

zone, these formations comprise more porous shallow-water 

carbonate facies, including digitate and planar algal bioherms, 

and as discussed previously, breccias associated with the 

shoulder of the Cambrian Reelfoot rift. In effect, to the east of 

the Wilderness-Handy fault zone, only an unconfined aquifer 

exists from the basement confining unit to the surface. See 

Lowell and others (2010, Stop 11) for additional discussion 

of the Wilderness-Handy fault zone and its influence on 

groundwater flow.

From the top of the St. Francois confining unit to the topographic surface is the Ozark aquifer (Imes, 1990a). In the map 

area it comprises, in ascending order, the Potosi, Eminence, 

and Gasconade Dolomites, the Roubidoux Formation, and 

the Jefferson City and Cotter Dolomites. The Ozark aquifer is 

unconfined and serves as the principal domestic water source 

for most of southeastern Missouri, except in the St. Francois 

Mountains, where near-surface stratigraphic units of the 

St. Francois aquifer are commonly tapped.

A hydrologic study of the Viburnum Trend mining district 

by Kleeschulte (2001) encompassed the northeastern part 

of the map area, including the area around the Sweetwater 

Mine, but did not extend to the Current River. The contoured 

potentiometric surface drawn by Kleeschulte (2001) shows 

a deep, southwest-inclined trough beneath Big Creek, 

which is a tributary to the Current River. In a more regional 

hydrologic study of south-central Missouri, Gann and others 

(1976) produced a slightly different potentiometric surface 

that depicted a relatively deep and narrow, southerly inclined 

groundwater trough beneath Logan Creek, with groundwater 

flow toward Blue Spring. Although Kleeschulte (2001) and 

Gann and others (1976) differ in exact locations of their potentiometric troughs, they clearly demonstrate that groundwater 

flow occurs from the southern part of the Viburnum Trend, 

in the Black River drainage basin (Sweetwater Mine area), 

and rapidly moves to the southwest toward the Current River. 

A study by Duchrow and others (1980) demonstrated that 

particulate material introduced into the Logan Creek surface 

drainage from three tailings-pond breaches in 1977 and 1978 

made their way into the Current River alluvial system via 

Blue Spring. Dye traces further indicate that the underground 

workings of the Sweetwater Mine are within the recharge area 

for springs along the Current River, particularly Blue Spring 

(Kleeschulte, 2001).

Dye-tracing studies conducted for springs southwest 

of the Current River (Aley, 1978; Aley and Aley, 1987; 

Kleeschulte, 2000; Imes and Kleeschulte, 1995; Imes and 

others, 2007) indicate that groundwater flow is commonly 

interconnected beneath surface drainage divides and is much 

more complicated than surface flow. For example, some 

groundwater dye-traces recovered at Big Spring originated 

more than 50 mi (80 km) away to the southwest and crossed 

beneath the entire Eleven Point River surface basin (fig. 2A) 

(Imes and Kleeschulte, 1995; Kleeschulte (2000). Measured 

in a direct line, these distant traces, as well as shorter traces, 

pass through the proposed prospecting-permit-application area 

in the flow path to Big Spring (Imes and Kleeschulte, 1995). 

The inconsistent pattern of crossing flow paths (see Imes and 
Discussion 15

Kleeschulte, 1995) is best explained by including an overriding karst control on groundwater flow. When the pattern 

of losing streams is added into consideration (see Imes and 

Kleeschulte, 1995), it is very clear that there is little consistency between surface-water flow and groundwater flow; once 

again, this is best explained by incorporating an overriding 

karst control over the regional hydrology.

To check for geologic controls on groundwater flow, 

particularly in areas of mapped fault structures, a potentiometric groundwater surface map of the Ozark aquifer was 

created (fig. 8) from water-table data provided by the USGS 

Missouri Water Science Center in Rolla (Imes and others, 

2007). Water levels from more than 300 wells, all measured 

during the same low-water- flow season (fall 2000), were 

contoured by hand. Contouring followed strict rules of 

interpolation between control points only, independent of 

all geology. Our contour data shows gross similar trends to 

that generated by Imes and Kleeschulte (1995) and Imes and 

others (2007); however, there are differences in detail due to 

differences in contouring methods used and to the fact that our 

contouring is more regional in coverage. 

Our contoured groundwater map (fig. 8) exhibits an 

irregular, undulating surface, consisting of an alternating series 

of northwest-trending subparallel troughs and ridges that are 

interrupted by a northeast-trending, elongated groundwater 

high that closely coincides with the Wilderness-Handy fault 

zone and its associated regional subsurface stratigraphic 

changes. These changes are related to the uplifted shoulder of 

the Reelfoot rift to the southeast of the map area, as discussed 

previously in the “Cambrian and Ordovician geologic 

history” section. Northwest of and adjacent to the elongated 

groundwater high are two prominent closed groundwater 

depressions that are connected by a trough in the water table. 

One depression is associated with the confluence of the Eleven 

Point River and both Spring and Hurricane Creeks and the 

other with the Pike Creek basin south of Fremont, about 9 mi 

(14 km) west-southwest of Big Spring. A similar trough is 

apparent in the potentiometric surface of Imes and Kleeschulte 

(1995), who first emphasized the necessity of groundwater 

flow through this trough in order to explain movement of 

dye traces to Big Spring. The potentiometric surface is also 

discussed in more detail in Lowell and others (2010).
16 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Description of Map Units

Paleozoic Sedimentary Rocks

Ocjc Cotter Dolomite and Jefferson City Dolomite, undivided (Lower Ordovician) —Dolomite, quartz 

sandstone, and chert. Dolomite is light brown, medium to fine grained, argillaceous, and thin to thick 

bedded; commonly weathers powdery-pale-yellow. Lenses of quartz sandstone and orthoquartzite 

as well as beds and nodules of white chert are also common. In some areas an interval of brown, 

medium-grained, thick-bedded to massive, siliceous, pitted-weathering dolomite informally known as 

the “Quarry Ledge” crops out. The “Quarry Ledge” occurs between 25 and 40 ft (8–12 m) above the 

base of the Jefferson City Dolomite, making it a useful marker for the Roubidoux-Jefferson City contact, 

which is seldom exposed. The Jefferson City Dolomite weathers to a characteristic yellowish color and 

produces a more silty, less sandy soil than the underlying Roubidoux Formation. Residual sandstone 

and orthoquartzite float from the Jefferson City are usually less tabular in shape than those produced 

from the Roubidoux. These characteristics enable differentiation between Roubidoux and Jefferson City 

bedrock in areas having no outcrop. The Jefferson City Dolomite is difficult to differentiate from the 

Cotter Dolomite without good exposure of the contact. Since exposures of either formation are rare in 

the study area, these units are undifferentiated. The Jefferson City and Cotter Dolomites are sparsely 

fossiliferous, but have yielded trilobites and conodonts as reported by Repetski and others (1998). 

These formations each have an average thickness of about 200 ft (61 m) in Missouri (Thompson, 1995). 

Typically considerably less than the full 400-ft (122-m) thickness of these combined units is exposed in 

the Current River and Eleven Point River basins. Areas underlain by the Cotter Dolomite are probably 

restricted to the southern and western uplands in the map area

Or Roubidoux Formation (Lower Ordovician) —Sandstone, orthoquartzite, dolomite, sandy dolomite, 

and chert. Sandstone is white to pale orange, fine to coarse grained, thin to thick bedded, generally 

poorly sorted, and commonly crossbedded and ripple marked; weathers light brown to reddish brown. 

Dolomite is light to medium gray, very fine to coarse grained, and thin to medium bedded. Chert is white 

to medium gray, locally sandy and oolitic; occurs in thin beds, lenses, and nodules. Typically formation 

is highly weathered and not well exposed. Thickness ranges up to as much as 250 ft (76 m)

Og Gasconade Dolomite (Lower Ordovician) —Dolomite, chert, sandstone, and orthoquartzite. Formation 

can be divided into three informal units (fig. 4), the lower, middle, and upper, which are not shown 

separately on this map. Upper unit is typically light-gray, medium- to coarse-grained, thick-bedded, 

vuggy dolomite. Weathered surfaces are commonly pitted. Middle unit is further divided into lower, 

middle, and upper parts. The upper part of the middle unit is typically light-gray, fine- to coarse-grained, 

medium- to thick-bedded dolomite, and contains white to light-gray chert nodules and lenses. The 

uppermost bed of the upper part of the middle unit is a persistent white Cryptozoon chert, 2 to 10 ft 

(0.6 –3 m) thick, commonly used to map the Roubidoux/Gasconade contact, which rarely is exposed. 

This contact is placed at approximately 80 to 100 ft (24–30 m) above the Cryptozoon chert, which is 

an average of observed intervals. The middle part of the middle unit is light-gray to very light gray, 

medium- to coarse-grained, medium-bedded dolomite containing chert as nodules, stringers, and beds. 

Chert varieties are porcelaneous, oolitic, porous with druse, and stromatolitic. A locally persistent oolite 

bed, occurring at the base of the middle part of the middle unit (Orndorff and Harrison, 2001), defined 

the top of the Van Buren Formation of Bridge (1930). Beds of the lower part of the middle unit, formerly 

called the Van Buren Formation by Bridge (1930), are light-gray to yellowish-gray, fine- to mediumgrained, thin- to medium-bedded dolomite. The lower unit of the Gasconade Dolomite, called the Gunter 

Sandstone Member, is a light-gray to white sandstone, sandy dolomite, or orthoquartzite interbedded 

with light-gray to tan, fine-grained, thin-bedded dolomite. The Gunter Sandstone Member ranges from 

10 to 25 ft (3–8 m) in thickness. In some localities the sandstones in the Gunter thin and exist only 

as discontinuous thin lenses. In some locations there is no quartz sandstone, making identification of 

the base of the Gasconade difficult. The thickness of the Gasconade Dolomite ranges from as much as 

about 770 ft (235 m) to as little as 148 ft (45 m) in areas adjacent to the Proterozoic volcanic knobs. The 

Gasconade is the youngest Paleozoic unit observed in contact with Mesoproterozoic igneous rocks in 

the Current River basin. Contact with the underlying Eminence Dolomite, which is unconformable, is 

placed at the base of the lowest sandstone or sandy dolomite of the Gunter Sandstone Member
Description of Map Units 17

_e Eminence Dolomite (Upper Cambrian) —Dolomite, sandstone, and chert. Dolomite is light gray, 

medium to coarse grained, massive to thick bedded, and commonly stromatolitic. It typically weathers 

bluish gray and medium gray, has a pitted surface, and commonly crops out as small knobs or pinnacles. 

Many fresh surfaces contain oxidized rust-colored mottles. Unit contains variable amounts of chert 

throughout, commonly as light-gray and white stringers and nodules. In downstream areas of the 

Current River basin, a 10- to 20-ft (3–9-m)-thick interval consisting of interbedded thin, friable to 

silicified quartz sandstone and sandy dolomite occurs 50 to 80 ft (15–24 m) below the upper contact. 

The thickness of the Eminence Dolomite is variable, in part because of the unconformity at the top 

of the unit and in part because of thinning near knobs of Mesoproterozoic volcanic rocks; thickness 

ranges from about 80 ft (24 m) to as much as about 919 ft (280 m). Contact with the underlying 

Potosi Dolomite is indistinct, a condition that is likely related to secondary alteration (silicification) 

rather than to primary deposition 

_p Potosi Dolomite (Upper Cambrian) —Dolomite with chert. Dolomite is light brown, brown, and light 

gray, fine to medium grained, massive to thick bedded, and contains quartz druse in vugs. Brown dolomite has fetid odor when freshly broken. Quartz druse is developed as botryoidal masses of chalcedony 

and small quartz crystals coating surfaces. White to light-gray chert forms nodules and stringers. 

Locally, a 1- to 3-ft (0.3–1-m)- thick bed of rusty-weathering porous chert occurs at or close to the 

contact with the overlying Eminence Dolomite. The Potosi ranges from about 50 to 575 ft (15–175 m) 

thick in the Current River basin

 Elvins Group (Upper Cambrian) —Consists of the Derby-Doerun Dolomite (usage of Missouri 

Geological Survey, 1979) and the Davis Formation

_dd Derby-Doerun Dolomite (usage of Missouri Geological Survey, 1979) (Upper Cambrian)—

Dolomite, siltstone, and shale. Dolomite is buff to light gray, fine to medium grained, thin to medium 

bedded, argillaceous and silty, and contains minor amounts of chert. Siltstone and shale are thin bedded 

and interbedded with dolomite. Lower part of unit is silty and glauconitic. Thickness averages about 

150 ft (46 m) but ranges up to about 354 ft (108 m)

_d Davis Formation (Upper Cambrian) —Shown in cross sections only. Shale, siltstone, sandstone, 

dolomite, and limestone conglomerate. Locally hydrothermally dolomitized to “white rock” that is 

indistinguishable from the overlying Derby-Doerun Dolomite (usage of Missouri Geological Survey, 

1979). Thickness averages about 170 ft (52 m) but ranges up to 322 ft (98 m) 

_b Bonneterre Formation (Upper Cambrian) —Shown in cross sections only. Interbedded dolomite, 

shale, limestone, and siltstone. Dolomite is light gray, fine to medium grained, medium bedded, locally 

glauconitic and argillaceous; lower part locally contains small igneous rock fragments where it was 

deposited directly over Mesoproterozoic basement rocks or near basement knobs. A shale interval 

2 to 6 ft (0.6–1.8 m) thick occurs in upper part of unit, and is commonly referred to as the “False 

Davis.” Limestone is brownish gray to pink, thin bedded, and fine grained. Siltstone is light to dark gray, 

laminated, and quartzose. Thickness about 564 ft (172 m)

_l Lamotte Sandstone (Upper Cambrian, Lower Cambrian?, and Neoproterozoic?) —Shown in cross 

sections only. Sandstone and conglomerate. Unit dominantly consists of light-gray to brown, mediumgrained, moderately to well-sorted quartzose sandstone. Coarse-grained basal conglomerate beds are 

common and consist of igneous detritus shed from knobs of Mesoproterozoic volcanic rocks. Clasts 

range in size up to boulders, several feet (1 m) in diameter. The exact age of basal conglomerate beds is 

poorly constrained and may be in part Lower Cambrian and (or) Neoproterozoic. Thickness ranges from 

zero at pinchouts against Mesoproterozoic knobs to about 330 ft (100 m)
18 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Mesoproterozoic Intrusive Rocks

Y2g Granite of Y2mg province of Sims (1990) and Graniteville-type granite of Kisvarsanyi (1981)—

Shown in cross sections only. Mesozonal granite. Van Schmus and others (1996) reported a uraniumlead (U-Pb) age of 1,323±6 Ma for this unit from an exploratory drill hole in Shannon County (see cross 

section A–A') in the map area and a U-Pb age of 1,376±4 Ma from a drill hole immediately south of the 

map area in Arkansas

Y1gb Gabbro of Sims (1990)—Shown in cross section B–B' only. YXgb gabbro unit of Sims (1990). Analyses 

by Van Schmus and others (1996) indicate a U-Pb age of ~1,500 Ma

Y1g Granite of Sims’ (1990) Y1g province and Kisvarsanyi’s (1981) Silvermine-Slabtown-type granite 

(Granite of Weary and McDowell (2006), known informally as Big Spring granite)—Granite, 

red, medium-grained and seriate, with clots of altered amphibole set in a semi-graphic intergrowth 

of quartz and alkali feldspar. The alkali feldspar exhibits Carlsbad twinning and some relict perthite 

of the herringbone type. Most perthite is disturbed and shows patch texture, chessboard character, 

and swapped rims. Accessory mineral phases include fluorite, zircon, and magnetite accompanied 

by secondary clay, sericite, and epidote. Outcrops are known from two areas in the map area, the 

Ellington 7.5-minute quadrangle (sec. 27, T. 29 N., R. 1 E.) and the Big Spring 7.5-minute quadrangle 

(sec. 29, T. 27 N., R. 1 E.). The outcrop in the Big Spring quadrangle (Weary and McDowell, 

2006) has a U-Pb age of 1,461.8 ± 5.5 Ma (Harrison and others, 2000). Other reported U-Pb ages 

from drill-hole samples collected in the map area for unit Y1g are 1,473 ± 15 Ma (Van Schmus and 

others, 1993) in the Van Buren South quadrangle (Weary and Schindler, 2004); 1,480±42 Ma 

(Van Schmus and others, 1993) in the Winona quadrangle (Orndorff and Harrison, 2001); and 

1,473 ± 15 Ma (Bickford and others, 1981) in the Round Spring quadrangle (Orndorff and Weary, 

2009). These ages are consistent with other reported ages for unit Y1g elsewhere in the Missouri Ozarks 

(see Van Schmus and others, 1993, and Bickford and others, 1981).

Y1gp Granite porphyry of Kisvarsanyi and Kisvarsanyi (1990)—Shown in cross section A‒A' only. 

Interpreted as a ring dike of the Eminence caldera by Kisvarsanyi and Kisvarsanyi (1990). Thickness of 

the ring dike is exaggerated in cross section A‒A' because the section cuts the granite body obliquely

Mesoproterozoic Volcanic Rocks

Y1v Volcanic rocks, undifferentiated—Shown in cross sections only

Upper Sequence of Mesoproterozoic Volcanic Rocks

Yr Rhyolite, undifferentiated—Exposed in a few small areas in the northeast corner of the study area, 

northeast of the Black fault

Yscr Rhyolite of Storys Creek—Alkali rhyolite named for a single exposure east of Storys Creek, in 

sec. 15, T. 29 N., R. 4 W. Rock is aphanophyric, with only 3 percent phenocrysts of alkali feldspar. 

Matrix texture is of the snowflake type and lacks both spherulites and lithophysal cavities. Fresh rock 

is medium pinkish gray. Thickness unknown

Yrm Rhyolite of Russell Mountain—Ash-flow tuff. Named for exposures on Russell Mountain, 

which spans sec. 2, T. 28 N., R. 2 W. of the Stegall Mountain 7.5-minute quadrangle (Harrison 

and others, 2002) and sec. 35, T. 29 N., R. 2 W. of the Powder Mill Ferry 7.5-minute quadrangle 

(McDowell and Harrison, 2000). Unit is moderately crystal rich, containing 10 to 20 percent (by 

volume) pink alkali feldspar phenocrysts that are locally altered pale green, sparse to no quartz, and 

5 to 10 percent magnetite and hematite grains. Unit is typically densely welded with well-developed 

flow banding and eutaxitic texture, although locally it is massive with poorly developed or no flow 

banding. This ash-flow tuff is interpreted to consist of multiple flows of both simple and compound 

cooling units. Primary foliations are typically steeply dipping and generally strike N. 40°–50° W. 
Description of Map Units 19

The steep dip of foliations (ranging from 25° to 90° and averaging about 76°; n=27) is interpreted to 

have been produced by rotation during caldera collapse (Harrison and others, 2000). Relation to the tuff 

of Little Thorny Mountain (Yltm) is uncertain but is possibly in part correlative. Thickness of this unit is 

difficult to determine because of rotation, but it is at least several thousand feet (1,000 m)

Yvc Volcaniclastic conglomerate, breccia, and sandstone—Interbedded volcaniclastic conglomerate, 

breccia, and sandstone. Conglomerate consists of subrounded cobbles, 3 to 5 in. (8–13 cm) in diameter, 

and large pebbles derived from the rhyolite of Sutton Creek (Ysc), upper unit of Coot Mountain 

(Ycu), and unidentified volcanic rocks. Matrix strongly altered, greenish, fine-grained volcaniclastic 

material. Conglomerate is overlain by strongly silicified volcanic breccia, possibly an autobrecciated 

flow, that consists of aphanitic pink rhyolite and quartz clasts in a quartz matrix. Sandstone is coarse 

to medium grained. Grains consist of quartz, lithics, and minor feldspar. Volcaniclastic unit observed 

only on southern side of Coot Mountain, in secs. 22 and 23, T. 29 N., R. 3 W., in the Eminence and 

Powder Mill Ferry 7.5-minute quadrangles (Orndorff and others, 1999; McDowell and Harrison, 2000). 

Contacts with other units not exposed

Ysc Rhyolite of Sutton Creek—Lava(?) of alkali rhyolite to rhyolite; massive and generally not flow 

layered, although flow layering is observed locally. Phenocrysts of 7 to 15 percent pink feldspar in a 

dark-pink matrix; 15 to 20 percent disseminated magnetite. Contains trace to 10 percent conspicuous, 

large (as much as 0.4 in.) (1 cm) aggregates (possibly xenoliths) of small pink feldspar phenocrysts in 

an apple-green matrix, which alter yellowish white. Named for exposures 0.4 km north of Sutton Creek 

in the Eminence 7.5-minute quadrangle (Orndorff and others, 1999), in sec. 12, T. 29 N., R. 4 W. Unit 

is also exposed along the northwest bank of the Current River in a knob 0.8 km southeast of the summit 

of Tip Top Mountain, and along the south bank of the Current River in an unnamed knob 1.6 km 

upstream from the confluence with the Jacks Fork River. Thickness unknown

Ysi Rhyolite of Shut-In Mountain—Dense lava of rhyolite to alkali trachyte. Named for exposures on 

and around Shut-In Mountain in the Stegall Mountain 7.5-minute quadrangle (secs. 2 and 11, T. 28 N., 

R. 3 W.). Unit is moderately crystal rich to crystal rich, with phenocrysts ranging from 12 to 30 percent 

by volume. This unit typically contains approximately 10 to 15 percent white to pink alkali feldspar; 

3 to 5 percent anhedral to euhedral quartz phenocrysts; common (but sporadic) blebs, pods, or 

disseminations of fluorite; and <1 to 3 percent disseminated magnetite-hematite grains in a dense, 

light-pink to maroon-red matrix that consists of a cryptocrystalline aggregate of quartz, alkali feldspar, 

and iron oxides. Flow banding is generally non-existent to poorly developed; however, where present 

it typically swirls and commonly displays flow folding. Locally, this unit is autobrecciated. Small 

zones of hydrothermal brecciation also occur locally. Vesicles mineralized with quartz and feldspar are 

common. This unit is interpreted as coalesced lava flows and domes. Areas of hydrothermal brecciation 

and inclusion of exotic aphanitic volcanic clasts are interpreted as marking probable vent sites. U-Pb 

analyses of one multiple-crystal fraction and five single-crystal fractions from this unit yielded an age 

of 1,470.4±2.7 Ma (Harrison and others, 2000). In part, this unit is the same as the Stegall Rhyolite of 

Tolman and Robertson (1969, p. 14–15). Minimum thickness 900 ft (275 m) 

Ysm Rhyolite of Stegall Mountain—Dense lava of rhyolite to alkali trachyte. Named for exposures on 

Stegall Mountain in secs. 19 and 20, T. 28 N., R. 2 W., in the Stegall Mountain 7.5-minute quadrangle 

(Harrison and others, 2002). This unit is a variation of the rhyolite of Shut-In Mountain in that it has 

a lower quartz phenocryst content of 0.5 to 2 percent. Otherwise, it is identical and is interpreted as 

genetically related. Minimum thickness 200 ft (61 m)

Ymm Tuff of Mule Mountain—Air-fall tuff. Unit is dense, aphanitic, finely laminated, and commonly 

silicified. Phenocrysts are rare and consist dominantly of angular quartz. Accretionary lapilli (lapillisize pellets of ash formed by rainfall through a downwind ash cloud or by accretion from a moistureladen eruption column) are relatively common. Base of unit marks an angular unconformity between 

the upper and lower sequences of volcanic rocks in the Stegall Mountain area. The contact with 

overlying units (Ysm and Ysi) is sharp and conformable. The contact with the underlying unit (Yltm) is 

complex and irregular. Unit was mapped only where its thickness exceeds 30 ft (9 m), but it is present 

everywhere between upper and lower sequences. Thickness ranges from 15 ft (4.5 m) to perhaps as 

much as 100 ft (30 m)
20 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Lower Sequence of Mesoproterozoic Volcanic Rocks 

Yltm Tuff of Little Thorny Mountain—Ash-flow tuff. Named for exposures on Little Thorny Mountain in 

the Stegall Mountain 7.5-minute quadrangle (Harrison and others, 2002), in sec. 22, T. 28 N., R. 2 W. 

Unit is dense, dark maroon to purple, moderately crystal rich to crystal rich, and quartz poor. Phenocryst 

content varies from 5 to 20 percent and consists almost exclusively of alkali feldspar; quartz is very 

rare to absent. Magnetite and hematite grains constitute 2 to 10 percent of the rock; fluorite blebs and 

disseminations are common. Sinha and Kisvarsanyi (1976) describe euhedral phenocrysts of relict 

fayalite, or possibly an iron pyroxene, which are now altered to hematite, calcite, sericite, and epidote. 

Unit contains fiamme and eutaxitic texture, is moderately to densely welded, and is commonly, but 

not everywhere, flow banded. Primary foliations are typically steeply dipping and generally strike 

N. 40°–50° W. Steeply dipping foliations are interpreted as having been produced by rotation during 

caldera collapse (Harrison and others, 2000). Thickness of unit is difficult to determine because of 

rotation, but it is at least several thousand feet (1,000 m)

Ycu Upper Coot Mountain unit—Rhyolite to alkali rhyolite to alkali trachyte ash-flow tuff, densely welded, 

with well-developed flow layering and eutaxitic texture; locally, flow layering is poorly developed. 

Primary foliations are typically steeply dipping. Generally less than 10 percent phenocrysts of pink 

feldspar and sparse to no quartz; 4 to 10 percent disseminated magnetite throughout; locally contains 

disseminated fluorite. Vapor-phase feldspar and quartz mineralization are common in pumice. Unit is 

exposed principally at the summit and along the northeast side of Coot Mountain, along the eastern side 

of Jerktail Mountain, and on the summit and slopes of Wildcat Mountain. Unit is approximately the 

same as the upper unit of Coot Mountain of Fisher (1969)

Ycl Lower Coot Mountain unit—Dominantly ash-flow tuff interbedded with air-fall tuff and lava(?). 

Ash-flow tuff is composed of alkali rhyolite to alkali trachyte to trachyte to rhyolite; commonly massive 

and dense. Flow layering weakly developed or nonexistent, although moderately developed locally. 

Five to 25 percent phenocrysts of pink feldspar and sparse to no quartz in a dark-maroon matrix, with 

4 to 10 percent disseminated magnetite throughout. Commonly contains quartz veins and infilling of 

miarolitic cavities, locally spherulitic. Locally, poorly welded to non-welded, pumice-rich, phenocrystpoor ash-flow tuff is interbedded in this interval. Ash-flow tuff is approximately the same as the middle 

unit of Coot Mountain of Fisher (1969). Air-fall tuff is composed of rhyolite; is aphanitic, massive to 

thin bedded, dark maroon, locally silicified, and contains disseminated pyrite. Petrographically consists 

of microlites less than 0.0004 in. (0.01 mm) in size and devitrified glass shards. Generally, all primary 

depositional features have been destroyed. Air-fall tuff is approximately the same as the lower unit of 

Coot Mountain of Fisher (1969). Unit is best exposed along the southwestern side of Coot Mountain, the 

western side of Jerktail Mountain, and on an unnamed knob exposed along Missouri Route 106, 2.0 km 

east of Eminence
References Cited 21

References Cited

Aley, T.J., 1978, A predictive hydrologic model for evaluating 

the effects of land use and management on the quantity and 

quality of water from Ozark springs: Missouri Speleology, 

v. 18, 185 p.

Aley, T.J., and Aley, Catherine, 1987, Groundwater study, 

Ozark National Scenic Riverways: Protem, Mo., Ozark 

Underground Laboratory, National Park Service contract 

CX 6000-4-0083, 222 p. 

Baker, H.W., 1999, Bedrock geologic map of the Grandin SW 

7.5-minute quadrangle: Missouri Geological Survey Map 

OFM-99-342-GS, 1 sheet, scale 1:24,000.

Bickford, M.E., Harrower, K.L., Hoppe, W.J., Nelson, B.K.,

Nusbaum, R.L., and Thomas, J.J., 1981, Rb-Sr and U-Pb 

geochronology and distribution of rock types in the 

Precambrian basement of Missouri and Kansas: Geological 

Society of America Bulletin, v. 92, p. 323–341.

Blakely, R.J., and Simpson, R.W., 1986, Approximating 

edges of source bodies from magnetic or gravity anomalies: 

Geophysics, v. 51, no. 7, p. 1494–1498.

Brezinski, D.K., 2000, Lower Mississippian trilobites from 

southern New Mexico: Journal of Paleontology, v. 74,

no. 6, p. 1043–1064.

Bridge, Josiah, 1930, Geology of the Eminence and Cardareva 

quadrangles: Missouri Geological Survey [Reports], 2d 

Series, v. 24, 228 p., 3 pls. in pocket, scale 1:62,500.

Cagniard, Louis, 1953, Basic theory of the magneto-telluric 

method of geophysical prospecting: Geophysics, v. 18,

no. 3, p. 605– 635.

Clendenin, C.W., and Duane, M.J., 1990, Focused fluid flow 

and Ozark Mississippi Valley-type deposits: Geology, v. 18, 

no. 2, p. 116–119.

Clendenin, C.W., Lowell, G.R., and Niewendorp, C.A., 1993, 

Sequencing Reelfoot extension based on relations from 

southeast Missouri and interpretations of the interplay 

between offset preexisting zones of weakness: Tectonics, 

v. 12 , no. 3, p. 703–712.

Clendenin, C.W., Niewendorp, C.A., and Lowell, G.R., 1989, 

Reinterpretation of faulting in southeast Missouri: Geology, 

v. 17, p. 217–220.

Cox, R.T., 2009, Ouachita, Appalachian, and ancestral

Rockies deformations recorded in mesoscale structures

on the foreland Ozark plateaus: Tectonophysics, v. 474,

no. 3– 4, p. 674– 683.

Craig, L.C., and Connor, C.W., coordinators, 1979, 

Paleotectonic investigations of the Mississippian System 

in the United States, Part III: U.S. Geological Survey 

Professional Paper 1010, pls. 1–15.

Dewey, J.W., Hill, D.P., Ellsworth, W.L., and Engdahl, E.R., 

1989, Earthquakes, faults, and the seismotectonic framework of the contiguous United States, in Pakiser, L.C., and 

Mooney, W.D., Geophysical framework of the continental 

United States: Geological Society of America Memoir 172, 

p. 541–575.

Diehl, S.F., Clendenin, C.W., and Lowell, G.R., 1995, The 

Ironton fault; additional observations and interpretations 

of the significance of a Precambrian mylonitic shear zone 

[abs.]: Geological Society of America Abstracts with 

Programs, v. 27, no. 6, p. 222.

Dmitriev, V.I., and Berdichevsky, M.N., 1979, The fundamental model of magnetotelluric sounding: Institute of 

Electrical and Electronics Engineers Proceedings, v. 67, 

no. 7, p. 1034–1044.

Dom, J.E., and Wicks, C.M., 2003, Morphology of the caves 

of Missouri: Journal of Cave and Karst Studies, v. 65, no. 3, 

p. 155–159.

Duchrow, R.M., Robinson-Wilson, E., and Trial, Linden, 

1980, The effects of lead mine tailings on the water

quality of Logan Creek, Reynolds County, Missouri:

Missouri Department of Conservation, 29 p.

Economic Geology, 1977, An issue devoted to the Viburnum 

Trend, southeast Missouri: Economic Geology, v. 72, no. 3, 

p. 337–490.

Epstein, A.G., Epstein, J.B., and Harris, L.D., 1977, Conodont 

color alteration; an index to organic metamorphism: U.S. 

Geological Survey Professional Paper 995, 27 p.

Feder, G.L., and Barks, J.H., 1972, A losing drainage 

basin in the Missouri Ozarks identified on side-looking 

radar imagery, in Geological Survey Research 1972: 

U.S. Geological Survey Professional Paper 800–C, 

p. C249–C252.

Fisher, H.H., 1969, Stratigraphy and correlation of 

Precambrian volcanic rocks, Eminence (Shannon County), 

Missouri: Rolla, Mo., University of Missouri-Rolla, 

unpublished M.S. thesis, 77 p.

Gann, E.E., Harvey, E.J., and Miller, D.E., 1976, Water 

resources of south-central Missouri: U.S. Geological Survey 

Hydrologic Investigations Atlas HA–550, 4 sheets.

Glazner, A.F., 1991, Plutonism, oblique subduction, and

continental growth; an example from the Mesozoic of

California: Geology, v. 19, no. 8, p. 784–786.
22 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Grohskopf, J.G., 1955, Subsurface geology of the Mississippi 

embayment of southeast Missouri: Missouri Geological

Survey and Water Resources [Reports], 2d Series, v. 37,

133 p.

Hadley, J.B., and Devine, J.F., 1974, Seismotectonic map 

of the eastern United States: U.S. Geological Survey 

Miscellaneous Field Studies Map MF–620, 3 sheets, 

scale 1:5,000,000.

Hagni, R.D., 1989, The southeast Missouri lead district;

a review, in Hagni, R.D., Coveney, R.M., Jr., and 

Thompson, T.B., eds., Mississippi Valley-type mineralization of the Viburnum Trend, Missouri: Society of 

Economic Geologists Guidebook Series, v. 5, p. 12–57.

Harrison, R.W., Lowell, G.R., and Unruh, D.M., 2000, 

Geology, geochemistry, and age of Mesoproterozoic 

igneous rocks in the Eminence-Van Buren area—A major 

structural outlier of the St. Francois terrane, south-central 

Missouri [abs.]: Geological Society of America Abstracts 

with Programs, v. 32, no. 3, p. A–14.

Harrison, R.W., and McDowell, R.C., 2003, Geologic map 

of the Wilderness and Handy quadrangles, Oregon, Carter, 

and Ripley Counties, Missouri: U.S. Geological Survey 

Geologic Investigations Series Map I–2801, scale 1:24,000.

Harrison, R.W., Orndorff, R.C., and Weary, D.J., 2002,

Geology of the Stegall Mountain 7.5-minute quadrangle, 

Shannon and Carter Counties, south-central Missouri:

U.S. Geological Survey Geologic Investigations Series

Map I–2767, scale 1;24,000.

Harrison, R.W., and Schultz, A.P., 2002, Tectonic framework 

of the southwestern margin of the Illinois basin and its 

influence on neotectonism and seismicity: Seismological 

Research Letters, v. 73, issue 75, p. 685–718.

He, Zhenhao, Gregg, J.M., Shelton, K.L., and Palmer, J.R., 

1997, Sedimentary facies control of fluid flow and mineralization in Cambro-Ordovician strata, southern Missouri, 

in Montañez, I.P., Gregg, J.M., and Shelton, K.L., eds., 

Basinwide diagenetic patterns; integrated petrologic, 

geochemical, and hydrologic considerations: Society for 

Sedimentary Geology Special Publication 57, p. 81–99.

Hedden, W.J., 1968, Bedrock geology of the Thayer 

7.5-minute quadrangle, Ripley County, Missouri: 

Unpublished data on file at the Missouri Geological 

Survey, Rolla, Mo., scale 1:24,000.

Hermann, R.B., and Nguyen, B., 1992, Seismological

investigation of earthquakes in the New Madrid seismic 

zone: U.S. Nuclear Regulatory Commission, Division of 

Engineering, Office of Nuclear Regulatory Research,

NRC FIN F1694, 62 p.

Hessler, R.R., 1963, Lower Mississippian trilobites of the

family Proetidae in the United States, Part I: Journal of 

Paleontology, v. 37, no. 3, p. 543–563.

Hessler, R.R., 1965, Lower Mississippian trilobites of the 

family Proetidae in the United States, Part II: Journal of 

Paleontology, v. 39, no. 2, p. 248–264.

Heyl, A.V., Odland, S.K., Moss, C.K., and Ryan, G.S., 1983, 

Mineral resource potential map of the Irish Wilderness 

Roadless Area, Oregon County, Missouri: U.S. Geological 

Survey Miscellaneous Field Studies Map MF–1511–A, 

scale 1:24,000.

Hildenbrand, T.G., and Hendricks, J.D., 1995, Geophysical 

setting of the Reelfoot rift and relations between rift structures and the New Madrid seismic zone: U.S. Geological 

Survey Professional Paper 1538–E, 30 p.

Hildenbrand, T.G., and Kucks, R.P., 1991, Total intensity

magnetic anomaly map of Missouri: U.S. Geological

Survey Open-File Report 91–573, scale 1:500,000. 

Hildenbrand, T.G., and Kucks, R.P., 1992, Filtered

magnetic anomaly maps of Missouri: U.S. Geological

Survey Geophysical Investigations Map GP–1000,

2 sheets, scale 1:1,000,000.

Hudson, M.R., 2000, Coordinated strike-slip and normal 

faulting in the southern Ozark dome of northern Arkansas; 

deformation in a late Paleozoic foreland: Geology, v. 28, 

no. 6, p. 511–514. 

Hutton, D.H.W., Dempster, T.J., Brown, P.E., and Becker, S.D.,

1990, A new mechanism of granite emplacement; intrusion 

in active extensional shear zones: Nature (London), v. 343, 

no. 6257, p. 452– 455.

Imes, J.L., 1989, Major geohydrologic units in and adjacent to 

the Ozark Plateaus province, Missouri, Arkansas, Kansas, 

and Oklahoma; basement confining unit: U.S. Geological 

Survey Hydrologic Investigations Atlas HA–711–B, 1 sheet, 

scale 1:750,000.

Imes, J.L., 1990a, Major geohydrologic units in and adjacent 

to the Ozark Plateaus province, Missouri, Arkansas, Kansas, 

and Oklahoma; Ozark aquifer: U.S. Geological Survey 

Hydrologic Investigations Atlas HA–711–E, 3 sheets, 

scale 1:750,000.

Imes, J.L., 1990b, Major geohydrologic units in and adjacent 

to the Ozark Plateaus province, Missouri, Arkansas, Kansas, 

and Oklahoma; St. Francois aquifer: U.S. Geological 

Survey Hydrologic Investigations Atlas HA–711–C, 

2 sheets, scale 1:750,000.

Imes, J.L., and Emmett, L.F., 1994, Geohydrology of the 

Ozark Plateaus aquifer system in parts of Missouri,

Arkansas, Oklahoma, and Kansas: U.S. Geological Survey 

Professional Paper 1414–D, 127 p.
References Cited 23

Imes, J.L., and Kleeschulte, M.J., 1995, Seasonal groundwater 

level changes (1990–93) and flow patterns in the Fristoe 

Unit of the Mark Twain National Forest, southern Missouri: 

U.S. Geological Survey Water-Resources Investigations 

Report 95– 4096, 1 sheet.

Imes, J.L., Plummer, L.N., Kleeschulte, M.J., and

Schumacher, J.G., 2007, Recharge area, base-flow and 

quick-flow discharge rates and ages, and general water

quality of Big Spring in Carter County, Missouri, 

2000–04: U.S. Geological Survey Scientific Investigations 

Report 2007–5049, 80 p.

Imes, J.L., and Smith, B.J., 1990, Areal extent, stratigraphic 

relation, and geohydrologic properties of regional geohydrologic units in southern Missouri: U.S. Geological Survey 

Hydrologic Investigations Atlas HA–711–I, 3 sheets, 

scale 1:750,000 and 1:1,000,000.

Kidwell, A.L., 1946, Reconnaissance mapping in the Des Arc 

area: Rolla, Mo., Missouri Geological Survey and Water 

Resources, unpublished map.

Kisvarsanyi, E.B., 1974, Operation basement; buried 

Precambrian rocks of Missouri; their petrology and structure: American Association of Petroleum Geologists 

Bulletin, v. 58, no. 4, p. 674–684.

Kisvarsanyi, E.B., 1975, Data on Precambrian in drill holes 

of Missouri including rock type and surface configuration: 

Missouri Geological Survey Report of Investigations 56, 

20 p.

Kisvarsanyi, E.B., 1981, Geology of the Precambrian St. 

Francois terrane, southeastern Missouri (Contribution to 

Precambrian Geology no. 8): Missouri Geological Survey 

Report of Investigations 64, 58 p.

Kisvarsanyi, E.B., 1984, The Precambrian tectonic framework 

of Missouri as interpreted from the magnetic anomaly map: 

Missouri Geological Survey, Contribution to Precambrian 

Geology 14, part B, 19 p.

Kisvarsanyi, E.B., 1988, Precambrian ring complexes and 

mineralization in southeast Missouri, in Kisvarsanyi, Geza, 

and Grant, S.K., eds., Proceedings volume, North America 

conference on tectonic control of ore deposits and the 

vertical and horizontal extent of ore systems: Rolla, Mo., 

University of Missouri-Rolla, p. 312–321.

Kisvarsanyi, E.B., and Kisvarsanyi, Geza, 1990, Alkaline 

granite ring complexes and metallogeny in the Middle

Proterozoic St. Francois terrane, southeastern Missouri, 

U.S.A., in Gower, C.F., Rivers, T., and Ryan, B., eds.,

Mid-Proterozoic Laurentia-Baltica: Geological Association 

of Canada Special Paper 38, p. 433–446.

Kisvarsanyi, Geza, 1977, The role of the Precambrian igneous 

basement in the formation of the stratabound lead-zinccopper deposits in southeast Missouri: Economic Geology, 

v. 72, no. 3, p. 435–442.

Kisvarsanyi, Geza, and Kisvarsanyi, E.B., 1976, Orthopolygonal tectonic patterns in the exposed and buried 

Precambrian basement of southeast Missouri, in

Hodgson, R.A., ed., Proceedings of the 1st International 

Conference on the New Basement Tectonics: Utah 

Geological Association Publication 5, p. 169–182.

Kleeschulte, M.J., 2000, Ground- and surface-water relations 

in the Eleven Point and Current River Basins, south-central 

Missouri: U.S. Geological Survey Fact Sheet 032–00, 6 p.

Kleeschulte, M.J., 2001, Effects of lead-zinc mining on 

groundwater levels in the Ozark aquifer in the Viburnum 

Trend, southeastern Missouri: U.S. Geological Survey 

Water-Resources Investigations Report 00‒4293, 28 p.

Kleeschulte, M.J., and Seeger, C.M., 2000, Depositional

environment, stratigraphy, and vertical hydraulic

conductivity of the St. Francois confining unit in the

Fristoe Unit of the Mark Twain National Forest, Missouri: 

U.S. Geological Survey Water-Resources Investigations 

Report 00–4037, 65 p.

Kleeschulte, M.J., and Seeger, C.M., 2001, Stratigraphy and 

vertical hydraulic conductivity of the St. Francois confining 

unit in townships 25–27 N. and ranges 01–02 W., southeastern Missouri: U.S. Geological Survey Water-Resources 

Investigations Report 2001–4270, 64 p.

Kolata, D.R., and Nelson, W.J., 1990, Tectonic history of the 

Illinois basin, in Leighton, M.W., Kolata, D.R., Oltz, D.F.,

and Eidel, J.J., eds., Interior cratonic basins: American 

Association of Petroleum Geologists Memoir 51, 

p. 263–285.

Kucks, R.P, and Hill, P.L., 2005, Missouri aeromagnetic and 

gravity maps and data—A Web site for distribution of 

data: U.S. Geological Survey Data Series 128, available at 

http://pubs.usgs.gov/ds/2005/128/missouri.htm.

Larsen, K.G., Clendenin, C.W., Mouat, M.M., Walker, W.T., 

and Taylor, D.R., 1979, Frank R. Milliken Mine of Ozark 

Lead Company new lead belt, southeast Missouri, in

Paarlberg, Norman, ed., Viburnum Trend; the 26th annual 

field trip of the Association of Missouri Geologists,

Sept. 28–29, 1979: Association of Missouri Geologists,

26th Annual Field Trip Guidebook, p. 63–74.

Lowell, G.R., 2000, Eruptive styles of Mesoproterozoic 

A-type calderas in southeastern Missouri, U.S.A: Revista 

Brasileira de Geociências, v. 30, no. 4, p. 745–748.
24 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Lowell, G.R., and Clendenin, C.W., 2003, Recognition of 

Mesoproterozoic ductile shear along the Black fault in 

southeastern Missouri [abs.]: Geological Society of America 

Abstracts with Programs, v. 35, no. 1, p. 70.

Lowell, G.R., Darnell, B.D., Young, G.J., and Clendenin, 

C.W., 1995, The Ironton fault; identification of a 

Proterozoic mylonitic shear zone [abs.]: Geological Society 

of America Abstracts with Programs, v. 27, no. 3, p. 69.

Lowell, G.R., and Harrison, R.W., 2001, The EminenceVan Buren volcanic series; a rift-related caldera [abs.]: 

Geological Society of America Abstracts with Programs, 

v. 33, no. 4, p. A-19.

Lowell, G.R., Harrison, R.W., and Unruh, D.M., 2005, 

Contrasting rift-margin volcanism in the St. Francois 

terrane of Missouri at 1.47 Ga [abs.]: Geochimica et 

Cosmochimica Acta, v. 69, no. 10S, p. A-81 (Abstracts 

of the 15th Annual V.M. Goldschmidt Conference).

Lowell, G.R., Harrison, R.W., Weary, D.J., Orndorff, R.C., 

Repetski, J.E., and Pierce, H.A., 2010, Rift-related volcanism and karst geohydrology of the southern Ozark dome, 

in Evans, K.R., and Aber, J.S., eds., From Precambrian rift 

volcanoes to the Mississippian shelf margin; geological 

field excursions in the Ozark Mountains: Geological 

Society of America Field Guide 17, p. 99–158. Digital 

Object Identifier: 10.1130/2010.0017(06).

Marcher, M.V., and Stearns, R.G., 1962, Tuscaloosa 

Formation in Tennessee: Geological Society of America 

Bulletin 73, no. 11, p. 1365–1386.

Maxwell, J.C., 1974, Water resources of the Current River 

Basin, Missouri: Rolla, Mo., University of Missouri-Rolla, 

Water Resources Research Center, 134 p.

McCracken, M.H., 1971, Structural features of Missouri:

Missouri Geological Survey and Water Resources Report

of Investigations 49, 99 p.

McDowell, R.C., 1998, Geologic map of the Greer quadrangle, Oregon County, Missouri: U.S. Geological Survey 

Geologic Investigations Series Map I–2618, scale 1:24,000.

McDowell, R.C., and Harrison, R.W., 2000, Geologic map

of the Powder Mill Ferry quadrangle, Shannon and

Reynolds Counties, Missouri: U.S. Geological Survey 

Geologic Investigations Series Map I–2722, scale 1:24,000. 

Middendorf, M.A., 1979, [Bedrock geology of the] Centerville 

[7.5-minute] quadrangle, Missouri: Missouri Geological 

Survey [map], Publication order no. RO7903, 1 sheet,

scale 1:24,000.

Middendorf, M.A., Thomson, K.C., Easson, G.L., and

Sumner, H.S., 1991, Bedrock geologic map of the 

Springfield 1°×2° quadrangle, Missouri: U.S. Geological 

Survey Miscellaneous Investigations Series Map I–2029,

1 sheet, scale 1:250,000.

Missouri Department of Natural Resources, n.d., Geologic 

well logs of Missouri: Jefferson City, Mo., Missouri

Department of Natural Resources, Water Resources Center, 

http://www.dnr.mo.gov/env/wrc/logmain/index.html.

Missouri Geological Survey, 1979, Geologic map of Missouri: 

Rolla, Mo., Missouri Division of Geology and Land Survey, 

scale 1:500,000.

Missouri Speleological Survey, 1977, Caves of Reynolds and 

Shannon Counties: Missouri Speleology, v. 17, nos. 1–2,

68 p.

Missouri Speleological Survey, 1982a, Caves of the Jacks 

Fork Valley: Missouri Speleology, v. 22, nos. 1–2, 62 p.

Missouri Speleological Survey, 1982b, Caves of the Current 

River Valley: Missouri Speleology, v. 22, nos. 3–4, 120 p.

Missouri Speleological Survey, 1984, Caves of Oregon 

County: Missouri Speleology, v. 24, nos. 1–2, 55 p.

Mouat, M.M., and Clendenin, C.W., 1975, Ozark Lead 

Company mine, Viburnum Trend, southeast Missouri: 

Missouri Geological Survey Report of Investigations 58,

p. 49–56.

Mouat, M.M., and Clendenin, C.W., 1977, Geology of the 

Ozark Lead Company mine, Viburnum Trend, southeast 

Missouri: Economic Geology, v. 72, no. 3, p. 395–407.

Nuttli, O.W., and Brill, K.G., Jr., 1981, Earthquake source 

zones in the central United States determined from historical 

seismicity, in Barstow, N.L., Brill, K.G., Jr., Nuttli, O.W.,

and Pomeroy, P.W., eds., An approach to seismic zonation 

for siting nuclear electric power generating facilities in the 

eastern United States: U.S. Nuclear Regulatory Commission 

Report NUREG/CR-1577, p. 98‒143.

Orndorff, R.C., 2003, Geologic map of the Fremont

quadrangle, Shannon, Carter, and Oregon Counties,

Missouri: U.S. Geological Survey Geologic Investigations 

Series Map I–2775, scale 1:24,000.

Orndorff, R.C., and Harrison, R.W., 1997, Preliminary

geologic map of the Spring Valley 30'×60' quadrangle, 

Missouri: U.S. Geological Survey Open-File Report 

97–434, 1 sheet, scale 1:100,000, and 8-p. text

Orndorff, R.C., and Harrison, R.W., 2001, Geologic map

of the Winona quadrangle, Shannon County, Missouri:

U.S. Geological Survey Geologic Investigations Series

Map I–2749, scale 1:24,000.
References Cited 25

Orndorff, R.C., Harrison, R.W., and Weary, D.J., 1999, 

Geologic map of the Eminence quadrangle, Shannon 

County, Missouri: U.S. Geological Survey Geologic 

Investigations Series Map I–2653, scale 1:24,000.

Orndorff, R.C., and Weary, D.J., 2009, Geologic map of

the Round Spring quadrangle, Shannon County, Missouri: 

U.S. Geological Survey Scientific Investigations Map 3073, 

scale 1:24,000.

Orndorff, R.C., Weary, D.J., and Harrison, R.W., 2006, 

The role of sandstone in the development of an Ozark 

karst system, south-central Missouri, in Harmon, R.S., 

and Wicks, C., eds., Perspectives on karst geomorphology, hydrology, and geochemistry; tribute volume to 

Derek C. Ford and William B. White: Geological Society

of America Special Paper 404, p. 31–38.

Orndorff, R.C., Weary, D.J., and Lagueux, K.M., 2000, 

Geographic information systems analysis of geologic 

controls on the distribution of dolines in the Ozarks of 

south-central Missouri, U.S.A.: Acta Carsologica, v. 29/2, 

p. 161–175.

Orndorff, R.C., Weary, D.J., and Šebela, Stanka, 2001, 

Geologic framework of the Ozarks of south-central 

Missouri; contributions to a conceptual model of karst, in

Kuniansky, E.L., ed., U.S. Geological Survey Karst Interest 

Group [Workshop] Proceedings, St. Petersburg, Florida, 

February 13–16, 2001: U.S. Geological Survey WaterResources Investigations Report 01–4011, p. 18–24.

Paarlberg, N.L., and Evans, L.L., 1975, Fletcher Mine

(St. Joe Minerals Corporation), Viburnum Trend, southeast Missouri: Missouri Geological Survey Report of 

Investigations 58, p. 41–47.

Paarlberg, N.L., and Evans, L.L., 1977, Geology of the 

Fletcher Mine, Viburnum Trend, southeast Missouri: 

Economic Geology, v. 72, no. 3, p. 391–397.

Palmer, A.N., 1991, Origin and morphology of limestone 

caves: Geological Society of America Bulletin, v. 103,

no. 1, p. 1–21.

Palmer, J.R., 1989, Late Upper Cambrian shelf depositional 

facies and history, southern Missouri, in Gregg, J.M., 

Palmer, J.R., and Kurtz, V.E., eds., Field guide to the

Upper Cambrian of southeastern Missouri; stratigraphy, 

sedimentology, and economic geology: Rolla, Mo., 

University of Missouri-Rolla, p. 1–24.

Pratt, W.P., Middendorf, M.A., Satterfield, I.R., and 

Gerdemann, P.E., 1992, Geologic map of the Rolla 

1°×2° quadrangle, Missouri: U.S. Geological Survey 

Miscellaneous Investigations Series Map I–1998,

scale 1:250,000.

Repetski, J.E., Loch, J.D., and Ethington, R.L., 1998, 

Conodonts and biostratigraphy of the Lower Ordovician 

Roubidoux Formation in and near the Ozark National 

Scenic Riverways, southeastern Missouri, in Santucci, V.L.,

and McClelland, Lindsay, eds., National Park Service 

Paleontological Research: National Park Service, Geologic 

Resources Division, Technical Report NPS/NRGRD/

GRDTR-98/01, p. 109–115.

Repetski, J.E., Orndorff, R.C., Weary, D.J., and Ethington, R.L.,

2000, Conodont biostratigraphy of the Eminence DolomiteGasconade Dolomite contact interval in the Missouri 

Ozarks [abs.]: Geological Society of America Abstracts

with Programs, v. 32, no. 3, p. A-39–A-40.

Román-Berdiel, Teresa, Gapais, Denis, and Brun, Jean-Pierre, 

1997, Granite intrusion along strike-slip zones in experiment and nature: American Journal of Science, v. 297,

no. 6, p. 651–678.

Satterfield, I.R., 1976, Reconnaissance geologic map of 

the Raymondville 15' quadrangle, Missouri: Missouri 

Department of Natural Resources, Division of Geology

and Land Survey, scale 1:62,500.

Schmidt, C.J., Smedes, H.W., and O’Neill, J.M., 1990, 

Syncompressional emplacement of the Boulder and Tobacco 

Root batholiths (Montana, USA) by pull-apart along old 

fault zones: Geological Journal, v. 25, no. 3–4, p. 305–318.

Šebela, Stanka, Orndorff, R.C., and Weary, D.J., 1999, 

Geological controls in the development of caves in the 

south-central Ozarks of Missouri, U.S.A.: Acta Carsologica, 

v. 28/2, p. 273–291.

Seeger, C.M., and Palmer, J.R., 1998, Synsedimentary 

tectonism in the St. Francois Mountains region, southeast Missouri, in Seeger, C.M., and Palmer, J.R., eds., 

Syndepositional tectonics during the late Upper Cambrian: 

Association of Missouri Geologists, 45th Annual Meeting 

and Field Trip [Guidebook], September 25 and 26, 1998, 

Farmington, Missouri, [24] p.

Sims, P.K., 1990, Precambrian basement map of the 

northern midcontinent, U.S.A.: U.S. Geological Survey 

Miscellaneous Investigations Series Map I–1853–A, 

1 sheet, scale 1:1,000,000.

Sims, P.K., and Peterman, Z.E., 1986, Early Proterozoic 

Central Plains orogen; a major buried structure in the northcentral United States: Geology, v. 14, no. 6, p. 488–491.

Sinha, B.N., and Kisvarsanyi, Geza, 1976, Precambrian 

volcanic rocks exposed on Stegall and Mule Mountains, 

Carter and Shannon Counties, Missouri, in Kisvarsanyi, E.B.,

ed., Studies in Precambrian geology of Missouri 

(Contribution to Precambrian Geology no. 6): Missouri 

Geological Survey Report of Investigations 61, p. 114–121.
26 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Spector, Allan, 1982, Interpretation of an aeromagnetic survey 

of parts of Shannon, Carter, Oregon, and Ripley Counties in 

southeastern Missouri: U.S. Geological Survey Open-File 

Report 82–832, 1 pl. and 20-p. text.

Starbuck, Edith, 1999, Bedrock geologic map of the Briar 

7.5-minute quadrangle: Missouri Geological Survey Map 

OFM-99-332-GS, 1 sheet, scale 1:24,000.

Taylor, D.R., 1983, Faulting as related to lead-zinc mineralization, west end of the Milliken Mine, Reynolds County, 

Missouri: Rolla, Mo., University of Missouri-Rolla,

unpublished M.S. thesis, 88 p.

Tikoff, Basil, and Teyssier, Christian, 1991, Dextral shearing 

in the east-central Sierra Nevada magmatic arc; implications 

for Late Cretaceous tectonics and passive emplacement of 

granite [abs.]: Geological Society of America Abstracts with 

Programs, v. 23, no. 5, p. A-176.

Thomas, W.A., 2006, Tectonic inheritance at a continental 

margin: GSA Today, v. 16, no. 2, p. 4–11.

Thompson, T.L., 1986, Paleozoic succession in Missouri; 

part 4, Mississippian System: Missouri Geological Survey 

Report of Investigations 70, 182 p.

Thompson, T.L., 1995, The stratigraphic succession in 

Missouri: Missouri Department of Natural Resources, 

Division of Geology and Land Survey, v. 40, 2d Series, 

revised, 190 p.

Tolman, C.F., and Robertson, F., 1969, Exposed Precambrian 

rocks in southeast Missouri (Contributions to Precambrian 

Geology no. 1): Missouri Geological Survey and Water 

Resources Report of Investigations 44, 68 p.

Van Schmus, W.R., Bickford, M.E., Sims, P.K., Anderson, R.R.,

Shearer, C.K., and Treves, S.B., 1993, Proterozoic geology 

of the western midcontinent basement, in Reed, J.C., Jr.,

and others, eds., Precambrian: Conterminous U.S., v. C-2

of The Geology of North America: Boulder, Colo., 

Geological Society of America, p. 239–259.

Van Schmus, W.R., Bickford, M.E., and Turek, A., 1996, 

Proterozoic geology of the east-central midcontinent basement, in van der Pluijm, B.A., and Catacosinos, P.A., eds., 

Basement and basins of eastern North America: Geological 

Society of America Special Paper 308, p. 7–32.

Wait, J.R., 1962, Theory of magneto-telluric fields: U.S. 

Department of Commerce, Journal of Research of the 

National Bureau of Standards—D., Radio Propagation,

v. 66D, no. 5, p. 509–541.

Weary, D.J., 2008a, Geologic map of the Cedargrove quadrangle, Dent and Shannon Counties, Missouri: U.S. 

Geological Survey Scientific Investigations Map 2980,

scale 1:24,000.

Weary, D.J., 2008b, Geologic map of the Piedmont Hollow 

quadrangle, Oregon County, Missouri: U.S. Geological 

Survey Scientific Investigations Map 2979, scale 1:24,000.

Weary, D.J., and McDowell, R.C., 2006, Geologic map 

of the Big Spring quadrangle, Carter County, Missouri: 

U.S. Geological Survey Scientific Investigations Map 2804, 

scale 1:24,000. 

Weary, D.J., and Orndorff, R.C., 2001, Physical controls on 

karst features in the Ozark Plateaus of Missouri, U.S.A., as 

determined by multivariate analyses in a geographic information system (GIS): Acta Carsologica, v. 30/2, p. 181–194.

Weary, D.J., and Orndorff, R.C., 2012, Geologic map of the 

Alley Spring quadrangle, Shannon County, Missouri: 

U.S. Geological Survey Scientific Investigations Map 3161, 

scale 1:24,000.

Weary, D.J., Orndorff, R.C., and Repetski, J.E., 2013, 

Geologic map of the Jam Up Cave and Pine Crest quadrangles, Shannon, Texas, and Howell Counties, Missouri: 

U.S. Geological Survey Scientific Investigations Map 3248, 

scale 1:24,000.

Weary, D.J., and Schindler, J.S., 2004, Geologic map of the 

Van Buren South quadrangle, Carter County, Missouri:

U.S. Geological Survey Geologic Investigations Series

Map I–2803, scale 1:24,000.

Weary, D.J., and Weems, R.E., 2004, Geologic map of the 

Van Buren North quadrangle, Carter, Reynolds, and 

Shannon Counties, Missouri: U.S. Geological Survey 

Geologic Investigations Series Map I–2802, scale 1:24,000.

Wedge, W.K., 1999, Bedrock geologic map of the Poynor 

7.5-minute quadrangle: Missouri Geological Survey 

Map OFM-99-348-GS, 1 sheet, scale 1:24,000.

Weems, R.E., 2002, Geologic map of the Low Wassie

quadrangle, Oregon and Shannon Counties, Missouri:

U.S. Geological Survey Geologic Investigations Series

Map I–2719, scale 1:24,000.

Weller, J.M., Williams, J.S., Bell, W.A., and others, 1948, 

Correlation of the Mississippian formations of North 

America: Geological Society of America Bulletin, v. 59,

no. 2, p. 91–196.

Zoback, M.D., and Zoback, M.L., 1991, Tectonic stress 

field of North America and relative plate motions, in

Slemmons, D.B., Engdahl, E.R., Zoback, M.D., and 

Blackwell, D.D., eds., Neotectonics of North America: 

Geological Society of America, p. 339–366.

Zoback, M.L., 1992, Stress field constraints on intraplate

seismicity in eastern North America: Journal of Geophysical 

Research, v. 97, iss. B8, p. 11,761–11,782.
Appendix 1. Summary of Drill-Hole Data for the Study Area 
28 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Bardley CF-1 SE1/4SE1/4 sec. 17, 

T. 24 N., R. 1 W.

4067110 670717 728 — — — 

Bartlett BT-2 SE1/4NE1/4 sec. 1, 

T. 27 N., R. 5 W.

4100496 638923 1,040 — — — 

Birch Tree 801-163 SE1/4NW1/4 sec. 34, 

T. 27 N., R. 4 W.

4092638 644352 942 — — — 

Bunker HA-3 SW1/4SE1/4 sec. 5, 

T. 31 N., R. 2 W.

4141028 660790 1,262 — — 842 

Bunker HA-13 NE1/4NE1/4 sec. 8, 

T. 31 N., R. 2 W.

4140290 661104 1,220 — — 839 

Bunker HA-23 NW1/4 sec. 6,

T. 32 N., R. 2 W.

4141578 659220 1,290 — — 790 

Bunker HA-24 SW1/4SW1/4 sec. 1, 

T. 31 N., R. 3 W.

4140903 656786 1,040 — — 860 

Bunker HA-25 SE1/4NW1/4 sec. 11, 

T. 31 N., R. 3 W.

4139945 655515 1,290 — — 895 

Bunker HA-29 NE1/4NW1/4 sec. 18, 

T. 31 N., R. 2 W.

4138642 658812 1,270 — — 920 

Corridon BF-8 SE1/4NE1/4 sec. 18, 

T. 32 N., R. 1 W.

4148545 669209 1,265 — — 995 

Corridon BF-11-119-

577

NE1/4NW1/4 sec. 7, 

T. 32 N., R. 1 W.

4150222 668531 1,245 — — — 

Corridon BF-116 NE1/4SW1/4 sec. 18, 

T. 32 N., R. 1 W.

4148003 668461 1,207 — — — 

Corridon BF-120 SE1/4NW1/4 sec. 7, 

T. 32 N., R. 1 W.

4149906 668442 1,150 — — — 

Corridon 60W100 SE1/4SE1/4 sec. 31, 

T. 32 N., R. 1 W.

4142991 669410 1,080 — — — 

Corridon 60W112 SE1/4NE1/4 sec. 31, 

T. 32 N., R. 1 W.

4143727 669118 1,180 — — — 

Corridon 60W155 NW1/4NE1/4 sec. 31, 

T. 32 N., R. 1 W.

4144184 668910 1,004 — — — 

Corridon 579 SW1/4NE1/4 sec. 19, 

T. 32 N., R. 1 W.

4146989 668818 1,163 — — — 

Corridon 584 SW1/4NE1/4 sec. 7, 

T. 32 N., R. 1 W.

4149916 668735 1,069 — — — 

Fremont PK-21 SW1/4NE1/4 sec. 33, 

T. 26 N., R. 2 W.

4082750 662452 925 — — — 

Fremont PK-26 SE1/4NW1/4 sec. 1, 

T. 26 N., R. 3 W.

4090820 657248 970 — — — 

Fremont PK-32 NW1/4SE1/4 sec. 7, 

T. 26 N., R. 2 W.

4088909 659322 875 — — — 

Fremont PK-34 NW1/4NE1/4 sec. 32, 

T. 26 N., R. 2 W.

4083013 660875 910 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 29

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –860

 –393

 –371

401

390

390

440

491

460

575

520

545

589

308

315

—

—

—

—

—

 –477

—

—

 –518

 –515

332

283

285

328

379

345

486

435

452

501

144

162

176

436

—

—

 –571

 –639

—

—

 –781

 –721

84

123

116

161

195

161

327

288

306

359

 –152

 –123

 –144

286

303

 –805

 –673

 –834

 –661

 –1,774

 –1,150

 –1,084

 –174

 –202

 –217

 –165

 –132

 –177

—

26

2

86

—

—

—

 –13

15

—

 –1,150

 –1,234

 –1,174

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

72

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,455

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,178

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,885

 –1,580

 –1,084

 –364

 –214

 –218

 –170

 –139

 –182

61

 –4

1

81

 –182

 –206

 –192

 –34

10

 –1,222

 –1,158

 –1,239

 –1,180

CF-1

BT-2

801-163

HA-3

HA-13

HA-23

HA-24

HA-25

HA-29

BF-8

BF-11-119-

577

BF-116

BF-120

60W100

60W112

60W155

579

584

PK-21

PK-26

PK-32

PK-34
30 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Fremont PK-40 NW1/4SE1/4 sec. 2, 

T. 26 N., R. 3 W.

4090683 655995 975 — — — 

Fremont SF-1 NE1/4NE1/4 sec. 28, 

T. 26 N., R. 2 W.

4084866 663163 975 — — — 

Fremont SF-2 NW1/4SE1/4 sec. 27, 

T. 26 N., R. 2 W.

4084159 664112 910 — — — 

Fremont SF-28 SW1/4SE1/4 sec. 6,

T. 26 N., R. 2 W.

4089942 659417 720 — — — 

Fremont SJ76W05 NW1/4NE1/4 sec. 11, 

T. 26 N., R. 2 W.

4089722 665822 631 — — — 

Fremont SJ77W02 SW1/4NE1/4 sec. 32, 

T. 27 N., R. 2 W.

4092563 661010 761 — — — 

Fremont SJ77W05 SW1/4SE1/4 sec. 23, 

T. 27 N., R. 3 W.

4095016 656130 808 — — — 

Fremont SJ77W06 NE1/4SW1/4 sec. 21, 

T. 27 N., R. 2 W.

4095220 662007 731 — — — 

Fremont SJ82W19 SE1/4SW1/4 sec. 23, 

T. 26 N., R. 3 W.

4085266 655875 790 — — — 

Fremont 801-13 NW1/4SE1/4 sec. 20, 

T. 26 N., R. 2 W.

4085452 660901 905 — — — 

Fremont 801-18 NW1/4NW1/4 sec. 32, 

T. 27 N., R. 2 W.

4092727 660276 780 — — — 

Fremont 801-22AD SE1/4NW1/4 sec. 30, 

T. 26 N., R. 2 W.

4084337 658889 980 — — — 

Fremont 801-24 SE1/4SW1/4 sec. 29, 

T. 27 N., R. 2 W.

4093371 660643 730 — — — 

Fremont 801-52AF SE1/4SW1/4 sec. 30, 

T. 26 N., R. 2 W.

4083781 658853 990 — — — 

Fremont 801-55 SW1/4NW1/4 sec. 36, 

T. 26 N., R. 3 W.

4083063 657132 795 — — — 

Fremont 801-89 SE1/4SW1/4 sec. 30, 

T. 26 N., R. 2 W.

4083494 658976 1,000 — — — 

Fremont 801-90 SE1/4NW1/4 sec. 31, 

T. 26 N., R. 2 W.

4082958 658853 970 — — — 

Fremont 801-91 NE1/4NW1/4 sec. 31, 

T. 26 N., R. 2 W.

4083217 658877 980 — — — 

Fremont 801-92 NE1/4SW1/4 sec. 31, 

T. 26 N., R. 2 W.

4082549 658867 990 — — — 

Fremont 76W7 NW1/4SE1/4 sec. 9, 

T. 26 N., R. 2 W.

4088886 662506 760 — 470 140 

Greer 801-15 SW1/4SE1/4 sec. 4,

T. 25 N., R. 3 W.

4080525 652777 635 — — — 

Greer 801-16 SE1/4NW1/4 sec. 18, 

T. 25 N., R. 3 W.

4077850 649271 905 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 31

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

—

—

 –548

—

—

—

—

—

—

—

—

 –368

—

 –469

—

 –471

 –507

 –474

 –512

 –398

 –600

 –620

 –842

 –648

 –692

 –667

 –665

 –750

 –701

 –621

 –580

 –515

—

 –465

—

 –535

 –512

 –539

 –577

 –545

 –598

 –476

 –659

 –682

 –902

 –771

 –834

 –762

 –882

 –799

 –742

 –768

 –756

 –771

 –738

 –725

 –729

 –730

 –692

 –765

 –813

 –776

 –846

 –576

 –897

 –907

 –1,175

 –1,256

 –1,280

—

 –1,180

—

 –1,070

 –1,135

 –1,175

 –1,163

 –1,160

 –1,124

 –1,126

 –1,198

 –1,136

—

 –1,213

 –1,175

 –1,224

 –1,117

 –1,334

 –1,334

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,189

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,185

 –1,325

 –1,312

 –1,212

 –1,317

 –1,045

 –1,104

 –1,155

 –1,458

 –1,165

 –1,183

 –1,167

 –1,137

 –1,210

 –1,152

 –1,165

 –1,248

 –1,193

 –1,233

 –1,155

—

—

PK-40

SF-1

SF-2

SF-28

SJ76W05

SJ77W02

SJ77W05

SJ77W06

SJ82W19

801-13

801-18

801-22AD

801-24

801-52AF

801-55

801-89

801-90

801-91

801-92

76W7

801-15

801-16
32 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Greer 801-17 SW1/4NE1/4 sec. 21, 

T. 25 N., R. 3 W.

4076347 652644 590 — — — 

Greer 801-51 SW1/4NE1/4 sec. 5, 

T. 25 N., R. 3 W.

4081147 651253 840 — — — 

Greer 801-54-BK SE1/4SW1/4 sec. 5,

T. 25 N., R. 3 W.

4080459 650746 920 — — — 

Greer 801-56 SW1/4SW1/4 sec. 12, 

T. 25 N., R. 4 W.

4078923 647041 920 — — — 

Greer 801-57 NE1/4NW1/4 sec. 2, 

T. 25 N., R. 4 W.

4081524 645781 980 — — — 

Greer 801-65-BC SE1/4NW1/4 sec. 2, 

T. 25 N., R. 3 W.

4081278 655613 950 — — — 

Greer 801-70 NE1/4SW1/4 sec. 15, 

T. 25 N., R. 3 W.

4077796 653861 640 — — — 

Greer 801-85 NE1/4NW1/4, sec. 2, 

T. 25 N., R. 3 W.

4081544 655357 920 — — — 

Greer 801-86 NE1/4NW1/4 sec. 21, 

T. 25 N., R. 3 W.

4076954 652151 790 — — — 

Greer 801-87 SE1/4SW1/4 sec. 13, 

T. 25 N., R. 4 W.

4077409 647490 890 — — — 

Greer 801-93 NE1/4SW1/4 sec. 24, 

T. 25 N., R. 4 W.

4075904 647531 580 — — — 

Greer 801-94 SW1/4NE1/4 sec. 4, 

T. 25 N., R. 3 W.

4081215 652643 640 — — — 

Greer 801-95 NE1/4SE1/4 sec. 9,

T. 25 N., R. 3 W.

4079307 653080 830 — — — 

Greer 801-106 SW1/4NE1/4 sec. 3, 

T. 25 N., R. 4 W.

4081232 644814 986 — — — 

Greer 801-114 SE1/4SE1/4 sec. 19, 

T. 25 N., R. 3 W.

4075517 649926 925 — — — 

Greer 801-117 NW1/4NW1/4 sec. 2, 

T. 25 N., R. 4 W.

4081534 645507 979 — — — 

Greer 801-118 SE1/4NE1/4 sec. 3,

T. 25 N., R. 4 W.

4081203 645240 960 — — — 

Greer 801-119 NW1/4NW1/4 sec. 1, 

T. 25 N., R. 4 W.

4081589 647049 960 — — — 

Greer 801-120 SE1/4SE1/4 sec. 12, 

T. 25 N., R. 4 W.

4079003 648254 920 — — — 

Greer 801-122 SW1/4SE1/4 sec. 2,

T. 25 N., R. 4 W.

4080589 646232 930 — — — 

Greer 801-123 SW1/4NE1/4 sec. 6, 

T. 25 N., R. 3 W.

4081281 649434 935 — — –272 

Greer 801-128 SE1/4NW1/4 sec. 12, 

T. 25 N., R. 4 W.

4079786 647637 940 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 33

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

—

 –590

 –550

 –531

 –507

 –547

 –519

 –642

 –623

 –606

 –613

 –639

 –675

 –547

 –639

 –553

 –561

 –586

 –608

 –593

 –584

 –604

 –581

 –652

 –614

 –594

 –571

 –612

 –585

 –701

 –698

 –663

 –710

 –706

 –753

 –646

 –683

 –647

 –673

 –653

 –678

 –703

 –682

 –685

 –831

 –906

 –899

 –877

 –864

 –849

 –823

 –905

 –908

 –932

 –931

 –919

 –949

 –855

 –949

 –861

 –871

 –877

 –902

 –895

 –889

 –899

 –1,334

 –1,388

 –1,328

 –1,313

 –1,247

 –1,290

 –1,261

 –1,342

 –1,353

 –1,340

 –1,368

 –1,346

 –1,387

 –1,277

 –1,379

 –1,261

 –1,286

 –1,286

 –1,327

 –1,312

 –1,314

 –1,326

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,345

 –1,347

—

—

 –1,307

 –1,286

 –1,365

—

 –1,358

 –1,382

 –1,362

 –1,391

—

 –1,403

—

—

 –1,298

 –1,348

—

 –1,328

—

801-17

801-51

801-54-BK

801-56

801-57

801-65-BC

801-70

801-85

801-86

801-87

801-93

801-94

801-95

801-106

801-114

801-117

801-118

801-119

801-120

801-122

801-123

801-128
34 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Greer 801-129 SW1/4SW1/4 sec. 2, 

T. 25 N., R. 4 W.

4080401 645446 855 — — — 

Greer 801-131 NW1/4NE1/4 sec. 11, 

T. 25 N., R. 4 W.

4079926 646381 890 — — — 

Greer 801-148 NW1/4SW1/4 sec. 11, 

T. 25 N., R. 4 W.

4079218 645607 920 — — — 

Greer 801-149 SW1/4SE1/4 sec. 3,

T. 25 N., R. 4 W.

4080327 644853 910 — — — 

Greer 801-156 SE1/4SE1/4 sec. 14, 

T. 25 N., R. 4 W.

4077174 646547 845 — — — 

Greer 801-158 SE1/4SW1/4 sec. 11, 

T. 25 N., R. 4 W.

4078789 646067 927 — — — 

Greer 82W3 NW1/4NW1/4 sec. 6, 

T. 25 N., R. 3 W.

4081570 648628 960 — — — 

Greer 83W25 NW1/4NE1/4 sec. 2, 

T. 24 N., R. 3 W.

4071621 655673 860 — — — 

Greer 84W40 SE1/4SE1/4 sec. 10, 

T. 25 N., R. 4 W.

4078893 645281 905 — — — 

Greer 84W44 NE1/4SW1/4 sec. 2, 

T. 24 N., R. 3 W.

4070766 655279 805 — — — 

Greer 85W9 NW1/4SE1/4 sec. 14, 

T. 25 N., R. 4 W.

4077702 646180 912 — — — 

Greer 85W11 NW1/4NE1/4 sec. 14, 

T. 25 N., R. 4 W.

4078380 646129 919 — — — 

Greer 85W15 NE1/4SE1/4 sec. 14, 

T. 25 N., R. 4 W.

4077645 646510 887 — — — 

Greer 85W31 NE1/4SE1/4 sec. 14, 

T. 25 N., R. 4 W.

4077822 646886 644 — — — 

Greer 86W2 NW1/4SE1/4 sec. 14, 

T. 25 N., R. 4 W.

4077673 646362 874 — — — 

Greer 86W4 SW1/4SW1/4 sec. 11, 

T. 25 N., R. 4 W.

4078811 645479 873 — — — 

Greer 86W6 SW1/4SW1/4 sec. 11, 

T. 25 N., R. 4 W.

4078723 645356 851 — — — 

Greer 88W4 SE1/4SE1/4 sec. 24, 

T. 25 N., R. 4 W.

4075793 648473 920 — — — 

Greer 88W5 SE1/4SE1/4, sec. 24, 

T. 25 N., R. 4 W.

4075505 648175 870 — — — 

Greer 88W6 SW1/4NE1/4, sec. 14, 

T. 25 N., R. 4 W.

4078035 646167 910 — — — 

Greer 89W1 SW1/4SW1/4 sec. 24, 

T. 25 N., R. 4 W.

4075612 647123 551 — — — 

Handy 81W29 NW1/4SW1/4 sec. 7, 

T. 24 N., R. 1 W.

4068822 667872 760 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 35

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –549

 –591

 –608

 –578

 –576

 –615

 –568

 –684

—

—

—

—

—

—

 –573

—

—

 –617

 –596

 –590

—

—

 –647

 –665

 –696

 –664

 –666

 –683

 –659

 –823

 –658

 –796

 –640

 –621

 –620

 –627

 –661

 –653

 –879

 –730

 –651

 –608

 –699

 –1,006

 –848

 –884

 –899

 –864

 –879

 –889

 –891

 –1,077

 –890

 –1,049

 –914

 –936

 –913

 –932

 –928

 –920

 –921

 –1,041

 –964

 –927

 –979

 –1,216

 –1,272

 –1,310

 –1,318

 –1,284

 –1,301

 –1,319

 –1,312

 –1,539

 –1,296

 –1,516

 –1,338

 –1,305

 –1,301

 –1,307

—

 –1,316

 –1,303

—

 –1,361

 –1,293

 –1,370

 –1,736

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,327

—

 –1,330

 –1,546

 –1,322

 –1,532

 –1,354

 –1,318

 –1,310

 –1,314

 –1,306

 –1,324

 –1,315

 –1,396

 –1,375

 –1,311

 –1,384

 –1,780

801-129

801-131

801-148

801-149

801-156

801-158

82W3

83W25

84W40

84W44

85W9

85W11

85W15

85W31

86W2

86W4

86W6

88W4

88W5

88W6

89W1

81W29
36 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Handy 76W3 SE1/4NW1/4 sec. 13, 

T. 25 N., R. 1 W.

4077855 676726 484 — — –236 

Handy 62W82 NE1/4SW1/4 sec. 5, 

T. 25 N., R. 1 W.

4080778 670230 600 — — — 

Handy 312-A SW1/4NW1/4 sec. 30, 

T. 25 N., R. 1 W.

4074729 668021 890 — — — 

Jam Up Cave MOSH-100 Sec. 7, T. 27 N.,

R. 5 W.

4098605 630027 ? — — — 

Loggers Lake HA-31 SE1/4NW1/4 sec. 4, 

T. 31 N., R. 3 W.

4141639 652510 1,210 — — 845 

Loggers Lake HA-33 SW1/4SE1/4 sec. 5,

T. 31 N., R. 3 W.

4140905 650931 1,170 — — 710 

Loggers Lake HA-34 NW1/4NW1/4 sec. 4, 

T. 31 N., R. 3 W.

4142420 651840 1,000 — — — 

Loggers Lake HA-35 NW1/4NW1/4 sec. 12,

T. 32 N., R. 4 W.

4150184 647488 1,210 — — 930 

Loggers Lake HA-36 SE1/4NW1/4 sec. 4, 

T. 31 N., R. 3 W.

4141769 652247 1,100 — — 1,065 

Loggers Lake HA-37 NE1/4NE1/4 sec. 4,

T. 31 N., R. 3 W.

4142324 653324 1,150 — — 965 

Low Wassie PK-9 SW1/4SW1/4 sec. 25, 

T. 27 N., R. 4 W.

4093501 646930 1,020 — — — 

Low Wassie PK-10 SW1/4NW1/4 sec. 12, 

T. 26 N., R. 4 W.

4089527 647057 1,000 — — — 

Low Wassie PK-13 SE1/4SE1/4 sec. 35, 

T. 27 N., R. 4 W.

4091567 646761 1,025 — — — 

Low Wassie PK-14 SW1/4NE1/4 sec. 9, 

T. 26 N., R. 3 W.

4089428 652941 1,005 — — — 

Low Wassie PK-15 NE1/4SE1/4 sec. 12, 

T. 26 N., R. 4 W.

4088885 648407 950 — — — 

Low Wassie PK-17 SE1/4SW1/4 sec. 12, 

T. 26 N., R. 4 W.

4088720 647585 990 — — — 

Low Wassie PK-18 NE1/4NW1/4 sec. 11, 

T. 26 N., R. 4 W.

4089841 645830 960 — — — 

Low Wassie PK-19 SE1/4NW1/4 sec. 28, 

T. 26 N., R. 3 W.

4084672 652533 925 — — — 

Low Wassie PK-20 SE1/4SW1/4 sec. 26, 

T. 26 N., R. 3 W.

4083833 655652 760 — — — 

Low Wassie PK-22 SE1/4SE1/4 sec. 11, 

T. 26 N., R. 4 W.

4088642 646798 935 — — — 

Low Wassie PK-23 SE1/4SW1/4 sec. 11, 

T. 26 N., R. 4 W.

4088700 645741 1,000 — — — 

Low Wassie PK-27 SW1/4SE1/4 sec. 35, 

T. 27 N., R. 4 W.

4091851 646086 1,000 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 37

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –796

—

 –733

—

510

305

575

497

650

563

—

—

—

—

—

—

—

—

—

 –377

 –347

 –318

 –1,182

 –1,015

 –1,001

—

465

203

449

387

539

447

—

 –378

—

 –514

 –502

 –396

 –327

 –560

 –553

 –470

 –488

 –509

 –1,206

 –1,071

 –1,299

—

335

21

275

203

374

276

 –693

 –581

 –689

 –715

 –697

 –596

 –525

 –751

 –715

 –682

 –732

 –710

 –1,607

 –1,453

 –1,705

—

—

 –307

 –58

 –120

—

 –51

 –1,085

—

 –1,045

 –1,154

 –1,097

 –920

 –647

 –1,185

 –1,195

 –1,074

 –1,112

 –1,095

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

?

43

—

—

—

136

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,683

 –1,988

 –1,752

?

38

 –355

 –69

 –175

97

 –135

 –1,104

 –879

 –1,092

 –1,159

 –1,190

 –924

 –647

 –1,199

 –1,255

 –1,085

 –1,160

 –1,109

76W3

62W82

312-A

MOSH-100

HA-31

HA-33

HA-34

HA-35

HA-36

HA-37

PK-9

PK-10

PK-13

PK-14

PK-15

PK-17

PK-18

PK-19

PK-20

PK-22

PK-23

PK-27
38 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Low Wassie PK-29 NW1/4NE1/4 sec. 28, 

T. 26 N., R. 3 W.

4085096 653006 1,016 — — — 

Low Wassie PK-30 NW1/4SW1/4 sec. 36, 

T. 27 N., R. 4 W.

4092156 647053 1,065 — — — 

Low Wassie PK-31 SW1/4NW1/4 sec. 6, 

T. 26 N., R. 3 W.

4090926 648732 990 — — — 

Low Wassie PK-33 NE1/4NE1/4 sec. 28, 

T. 26 N., R. 3 W.

4084820 653105 950 — — — 

Low Wassie PK-38 NE1/4SE1/4 sec. 29, 

T. 26 N., R. 3 W.

4084080 651771 875 — — — 

Low Wassie PK-41 NE1/4NE1/4 sec. 12, 

T. 26 N., R. 4 W.

4089691 648271 955 — — — 

Low Wassie PK-42 SE1/4NE1/4 sec. 12, 

T. 26 N., R. 4 W.

4089403 648082 915 — — — 

Low Wassie PK-43 SW1/4SW1/4 sec. 25, 

T. 27 N., R. 4 W.

4093267 646938 1,025 — — — 

Low Wassie PK-44 NW1/4SW1/4 sec. 25, 

T. 27 N., R. 4 W.

4093662 646946 1,010 — — — 

Low Wassie PK-46 SE1/4SW1/4 sec. 12, 

T. 26 N., R. 4 W.

4088404 647555 990 — — — 

Low Wassie SF-6 SE1/4SE1/4 sec. 34, 

T. 27 N., R. 3 W.

4092012 654969 985 — — — 

Low Wassie 76W20 SW1/4NE1/4 sec. 22, 

T. 27 N., R. 3 W.

4095876 654316 951 — — — 

Low Wassie 77W11 SW1/4NW1/4 sec. 21, 

T. 27 N., R. 3 W.

4095933 652237 901 — — — 

Low Wassie 79W03 SW1/4NW1/4 sec. 34, 

T. 27 N., R. 3 W.

4092563 653706 871 — — — 

Low Wassie 79W05 SW1/4NW1/4 sec. 35, 

T. 26 N., R. 3 W.

4082928 655265 706 — — — 

Low Wassie 82W21 SW1/4SW1/4 sec. 22, 

T. 26 N., R. 3 W.

4085285 653623 970 — — — 

Low Wassie 82W25 SW1/4NW1/4 sec. 22, 

T. 26 N., R. 3 W.

4086207 653776 965 — — — 

Low Wassie 82W27 SE1/4NW1/4 sec. 29, 

T. 26 N., R. 3 W.

4084475 650916 890 — — — 

Low Wassie 83W14 NW1/4SW1/4 sec. 22, 

T. 26 N., R. 3 W.

4085771 653628 985 — 465 95 

Low Wassie 83W15 SE1/4SW1/4 sec. 22, 

T. 26 N., R. 3 W.

4085326 654138 785 — — — 

Low Wassie 766-002 NW1/4SE1/4 sec. 6, 

T. 26 N., R. 3 W.

4090674 649499 1,022 — — — 

Low Wassie 801-002 NW1/4SW1/4 sec. 33, 

T. 27 N., R. 3 W.

4092111 652133 1,006 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 39

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

—

—

 –392

—

—

—

—

—

—

—

 –428

 –304

 –442

 –494

 –566

—

—

 –285

 –297

 –349

 –403

 –439

—

—

 –552

 –398

 –629

—

 –497

 –517

 –540

 –422

 –577

 –493

 –545

 –545

 –624

—

 –575

 –605

 –357

 –488

 –473

 –489

 –504

 –677

 –711

 –590

 –845

 –675

 –573

 –709

 –694

 –625

 –730

 –636

 –763

 –859

 –947

 –487

 –778

 –805

 –497

 –668

 –685

 –730

 –603

 –1,083

 –1,110

 –798

 –1,259

 –1,095

 –1,075

 –1,051

 –1,033

—

 –1,145

 –956

 –1,066

 –1,187

 –1,324

—

 –1,187

 –1,233

—

 –1,107

 –1,090

 –1,125

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,028

—

—

—

—

—

 –558

—

—

 –563

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,161

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –640

 –1,096

 –1,124

 –810

 –1,297

 –1,119

 –1,089

 –1,108

 –1,125

 –1,045

 –1,176

—

—

—

—

 –558

 –1,206

 –1,265

 –565

 –1,176

—

—

PK-29

PK-30

PK-31

PK-33

PK-38

PK-41

PK-42

PK-43

PK-44

PK-46

SF-6

76W20

77W11

79W03

79W05

82W21

82W25

82W27

83W14

83W15

766-002

801-002
40 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Low Wassie 801-003 NW1/4SE1/4 sec. 7, 

T. 26 N., R. 3 W.

4089070 649707 886 — — — 

Low Wassie 801-005 NE1/4NE1/4 sec. 26, 

T. 26 N., R. 4 W.

4085005 646847 820 — — — 

Low Wassie 801-009 SW1/4SE1/4 sec. 3,

T. 26 N., R. 4 W.

4090222 644733 895 — — — 

Low Wassie 801-011 SE1/4SE1/4 sec. 18, 

T. 26 N., R. 3 W.

4087120 650081 895 — — — 

Low Wassie 801-19-W SW1/4SW1/4 sec. 16, 

T. 26 N., R. 3 W.

4086811 651978 950 — — — 

Low Wassie 801-20 NW1/4SE1/4 sec. 20, 

T. 26 N., R. 3 W.

4085659 651369 920 — — — 

Low Wassie 801-21-AB NE1/4SE1/4 sec. 21, 

T. 26 N., R. 3 W.

4085898 653459 975 — — — 

Low Wassie 801-25-O NE1/4NW1/4 sec. 17, 

T. 26 N., R. 3 W.

4088350 650826 940 — — — 

Low Wassie 801-27-E NW1/4NW1/4 sec. 14,

T. 26 N., R. 4 W.

4088293 645630 990 — — — 

Low Wassie 801-28-H NE1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4088153 647477 985 — — — 

Low Wassie 801-29-O NW1/4NE1/4 sec. 19, 

T. 26 N., R. 3 W.

4086503 649489 920 — — — 

Low Wassie 801-30-P NW1/4SW1/4 sec. 19, 

T. 26 N., R. 3 W.

4085766 648563 880 — — — 

Low Wassie 801-31-BW NE1/4NE1/4 sec. 35, 

T. 26 N., R. 4 W.

4083191 646679 920 — — — 

Low Wassie 801-32-N NE1/4NW1/4 sec. 17, 

T. 26 N., R. 3 W.

4088058 650797 920 — — — 

Low Wassie 801-33-1 SW1/4NE1/4 sec. 7, 

T. 26 N., R. 3 W.

4089428 649509 880 — — — 

Low Wassie 801-34-X SW1/4SW1/4 sec. 16, 

T. 26 N., R. 3 W.

4087025 651941 930 — — — 

Low Wassie 801-35-R NW1/4NE1/4 sec. 19, 

T. 26 N., R. 3 W.

4086589 649694 880 — — — 

Low Wassie 801-36-V NE1/4NE1/4 sec. 20, 

T. 26 N., R. 3 W.

4086540 651768 970 — — — 

Low Wassie 801-37-U NE1/4NE1/4 sec. 20, 

T. 26 N., R. 3 W.

4086367 651509 1,035 — — — 

Low Wassie 801-38 SW1/4NW1/4 sec. 17, 

T. 26 N., R. 3 W.

4087778 650649 920 — — — 

Low Wassie 801-39-L NW1/4SW1/4 sec. 17, 

T. 26 N., R. 3 W.

4087552 650336 830 — — — 

Low Wassie 801-40-AA NE1/4SE1/4 sec. 21, 

T. 26 N., R. 3 W.

4085622 653471 980 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 41

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –398

 –525

 –487

 –335

 –420

 –426

 –409

 –411

 –406

 –445

 –507

 –486

 –545

 –451

 –407

 –443

 –456

 –402

 –379

 –409

 –362

 –327

 –459

 –610

 –530

 –396

 –477

 –511

 –467

 –474

 –526

 –507

 –574

 –574

 –622

 –485

 –485

 –481

 –503

 –427

 –445

 –483

 –425

 –385

 –677

 –802

 –740

 –587

 –732

 –705

 –713

 –686

 –728

 –714

 –778

 –782

 –844

 –699

 –690

 –701

 –716

 –641

 –650

 –700

 –631

 –645

 –1,081

 –1,229

 –1,114

—

 –1,113

—

 –1,110

 –1,106

 –1,116

 –1,062

 –1,153

 –1,208

 –1,260

 –1,111

 –1,059

 –1,182

 –1,129

—

—

 –1,137

 –991

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,101

—

—

—

—

—

—

—

—

—

—

—

 –1,010

 –1,050

—

—

 –934

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,130

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,130

 –1,106

 –1,136

 –1,108

 –1,146

 –1,070

 –1,182

 –1,215

 –1,270

 –1,113

 –1,097

 –1,186

 –1,140

 –1,012

 –1,055

 –1,157

 –1,002

 –965

801-003

801-005

801-009

801-011

801-19-W

801-20

801-21-AB

801-25-O

801-27-E

801-28-H

801-29-O

801-30-P

801-31-BW

801-32-N

801-33-1

801-34-X

801-35-R

801-36-V

801-37-U

801-38

801-39-L

801-40-AA
42 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Low Wassie 801-41-Y NW1/4SW1/4 sec. 16, 

T. 26 N., R. 3 W.

4087313 652179 960 — — — 

Low Wassie 801-43-BA SW1/4SE1/4 sec. 20, 

T. 26 N., R. 3 W.

4085330 651398 905 — — — 

Low Wassie 801-44-T SW1/4NE1/4 sec. 20, 

T. 26 N., R. 3 W.

4085989 651472 970 — — — 

Low Wassie 801-45-G NW1/4NW1/4 sec. 13,

T. 26 N., R. 4 W.

4088248 647011 940 — — — 

Low Wassie 801-46-F NE1/4NE1/4 sec. 14, 

T. 26 N., R. 4 W.

4088157 646596 840 — — — 

Low Wassie 801-48 SW1/4SE1/4 sec. 15, 

T. 26 N., R. 4 W.

4087058 644864 890 — — — 

Low Wassie 801-49-J NW1/4NE1/4 sec. 32, 

T. 27 N., R. 3 W.

4093098 651188 1,030 — 335 –75 

Low Wassie 801-50-Z SE1/4SE1/4 sec. 21, 

T. 26 N., R. 3 W.

4085466 653212 960 — — — 

Low Wassie 801-58 NE1/4NE1/4 sec. 35, 

T. 26 N., R. 4 W.

4083387 646848 920 — — — 

Low Wassie 801-59 SE1/4SW1/4 sec. 2,

T. 26 N., R. 4 W.

4090016 645716 985 — — — 

Low Wassie 801-60 SE1/4SE1/4 sec. 7,

T. 26 N., R. 3 W.

4088745 650126 865 — — — 

Low Wassie 801-61 SE1/4SE1/4 sec. 7,

T. 26 N., R. 3 W.

4088432 649978 855 — — — 

Low Wassie 801-63 NE1/4NE1/4 sec. 13, 

T. 26 N., R. 4 W.

4088153 648423 980 — — — 

Low Wassie 801-66 SW1/4SW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087243 647123 915 — — — 

Low Wassie 801-67 NW1/4SW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087313 647074 945 — — — 

Low Wassie 801-68 NE1/4NE1/4 sec. 15, 

T. 26 N., R. 4 W.

4088161 644955 900 — — — 

Low Wassie 801-69-CP NW1/4SW1/4 sec. 19, 

T. 26 N., R. 3 W.

4085746 648682 885 — — — 

Low Wassie 801-71 NW1/4NW1/4 sec. 17,

T. 26 N., R. 3 W.

4087906 650661 930 — — — 

Low Wassie 801-72 NE1/4NW1/4 sec. 17, 

T. 26 N., R. 3 W.

4088124 650822 930 — — — 

Low Wassie 801-74 SE1/4NW1/4 sec. 19, 

T. 26 N., R. 3 W.

4086038 649003 900 — — — 

Low Wassie 801-75 SE1/4NW1/4 sec. 19, 

T. 26 N., R. 3 W.

4086110 649212 830 — — — 

Low Wassie 801-76 NE1/4NE1/4 sec. 27, 

T. 27 N., R. 4 W.

4094466 645112 1,090 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 43

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –458

 –463

 –327

 –418

 –454

 –447

 –425

 –395

 –568

 –332

 –432

 –429

 –368

 –515

 –472

 –475

 –497

 –424

 –428

 –493

 –464

 –448

 –512

 –560

 –390

 –487

 –525

 –578

 –480

 –460

 –650

 –405

 –495

 –501

 –435

 –586

 –584

 –552

 –585

 –497

 –500

 –580

 –549

 –557

 –725

 –762

 –578

 –711

 –737

 –772

 –682

 –663

 –852

 –642

 –685

 –694

 –652

 –806

 –783

 –739

 –790

 –703

 –698

 –782

 –757

 –715

 –1,138

 –1,181

—

 –1,059

 –1,097

 –1,122

 –1,069

 –1,090

 –1,268

 –972

 –1,087

 –1,116

—

 –1,205

 –1,191

 –1,133

 –1,210

 –1,168

 –1,123

 –1,198

 –1,171

 –1,052

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –768

—

—

—

—

—

—

—

—

—

 –951

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,160

 –1,201

 –814

 –1,067

 –1,127

 –1,148

 –1,107

 –1,112

 –1,275

—

—

—

 –992

 –1,222

 –1,103

 –1,162

 –1,232

 –1,170

 –1,138

 –1,208

 –1,184

 –1,062

801-41-Y

801-43-BA

801-44-T

801-45-G

801-46-F

801-48

801-49-J

801-50-Z

801-58

801-59

801-60

801-61

801-63

801-66

801-67

801-68

801-69-CP

801-71

801-72

801-74

801-75

801-76
44 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Low Wassie 801-77 SE1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087927 647128 985 — — — 

Low Wassie 801-78 SW1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087495 647007 940 — — — 

Low Wassie 801-79 NE1/4NE1/4 sec. 13, 

T. 26 N., R. 4 W.

4088155 648181 950 — — — 

Low Wassie 801-80 SE1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087918 647456 975 — — — 

Low Wassie 801-81 NE1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4088069 647628 960 — — — 

Low Wassie 801-82 NE1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4088164 647326 955 — — — 

Low Wassie 801-83 NW1/4NW1/4 sec. 13,

T. 26 N., R. 4 W.

4088190 647214 920 — — — 

Low Wassie 801-84 NW1/4NE1/4 sec. 13, 

T. 26 N., R. 4 W.

4088138 647879 920 — — — 

Low Wassie 801-88 NW1/4SW1/4 sec. 8, 

T. 26 N., R. 3 W.

4088846 650425 870 — — — 

Low Wassie 801-96 NW1/4SE1/4 sec. 24, 

T. 26 N., R. 4 W.

4085531 647797 910 — — — 

Low Wassie 801-97 SW1/4SE1/4 sec. 24, 

T. 26 N., R. 4 W.

4085212 647736 890 — — — 

Low Wassie 801-98 NE1/4NW1/4 sec. 25, 

T. 26 N., R. 4 W.

4085000 647426 840 — — — 

Low Wassie 801-99 NW1/4SW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087275 647266 900 — — — 

Low Wassie 801-100 NE1/4SW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087538 647382 900 — — — 

Low Wassie 801-101 SE1/4NW1/4 sec. 13, 

T. 26 N., R. 4 W.

4087789 647460 960 — — — 

Low Wassie 801-102 NW1/4NE1/4 sec. 19, 

T. 26 N., R. 3 W.

4086377 649359 910 — — — 

Low Wassie 801-103 NW1/4SW1/4 sec. 17, 

T. 26 N., R. 3 W.

4087530 650477 860 — — — 

Low Wassie 801-104 NW1/4NE1/4 sec. 13, 

T. 26 N., R. 4 W.

4087905 647780 900 — — — 

Low Wassie 801-107 NW1/4NE1/4 sec. 14, 

T. 26 N., R. 4 W.

4088181 646152 950 — — — 

Low Wassie 801-108 NW1/4SW1/4 sec. 17, 

T. 26 N., R. 3 W.

4087470 650400 840 — — — 

Low Wassie 801-109 SW1/4SE1/4 sec. 18, 

T. 26 N., R. 3 W.

4086981 650128 910 — — — 

Low Wassie 801-110 SE1/4SE1/4 sec. 18, 

T. 26 N., R. 3 W.

4086800 649877 900 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 45

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –468

 –502

 –390

 –475

 –433

 –419

 –425

 –431

 –418

 –519

 –509

 –545

 –487

 –481

 –453

 –480

 –431

 –434

 –462

 –381

 –327

 –396

 –537

 –565

 –451

 –540

 –507

 –197

 –489

 –505

 –481

 –582

 –596

 –617

 –546

 –548

 –528

 –550

 –496

 –502

 –549

 –441

 –402

 –459

 –738

 –778

 –655

 –738

 –709

 –700

 –696

 –713

 –667

 –785

 –796

 –830

 –752

 –745

 –740

 –739

 –681

 –708

 –744

 –633

 –582

 –650

 –1,080

 –1,185

 –1,051

 –1,092

 –1,107

 –1,087

 –1,048

 –1,115

 –1,077

 –1,209

 –1,214

 –1,243

 –1,170

 –1,152

 –1,145

 –1,156

—

 –1,121

 –1,156

—

 –821

 –1,032

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –985

—

—

 –1,039

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –834

 –1,042

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,103

 –1,195

 –1,086

 –1,103

 –1,124

 –1,103

 –1,069

 –1,133

 –1,104

 –1,218

 –1,221

 –1,256

 –1,185

 –1,173

 –1,164

 –1,178

 –994

 –1,158

 –1,188

 –1,042

—

—

801-77

801-78

801-79

801-80

801-81

801-82

801-83

801-84

801-88

801-96

801-97

801-98

801-99

801-100

801-101

801-102

801-103

801-104

801-107

801-108

801-109

801-110
46 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Low Wassie 801-111 NW1/4SW1/4 sec. 7, 

T. 26 N., R. 3 W.

4088859 648751 880 — — — 

Low Wassie 801-112 SE1/4SW1/4 sec. 7,

T. 26 N., R. 3 W.

4088406 649079 930 — — — 

Low Wassie 801-115 NE1/4NW1/4 sec. 14, 

T. 26 N., R. 4 W.

4088244 645852 960 — — — 

Low Wassie 801-116 NW1/4NE1/4 sec. 14, 

T. 26 N., R. 4 W.

4088177 646329 945 — — — 

Low Wassie 801-121 NE1/4SW1/4 sec. 36, 

T. 26 N., R. 4 W.

4082406 647624 940 — — — 

Low Wassie 801-124 SW1/4NE1/4 sec. 31, 

T. 26 N., R. 3 W.

4082890 649603 900 — — — 

Low Wassie 801-125 SE1/4NE1/4 sec. 34, 

T. 27 N., R. 4 W.

4092687 645028 1,020 — — — 

Low Wassie 801-126 NE1/4NE1/4 sec. 14, 

T. 26 N., R. 4 W.

4088242 646802 945 — — — 

Low Wassie 801-127 NE1/4NW1/4 sec. 14, 

T. 26 N., R. 4 W.

4088242 645766 990 — — — 

Low Wassie 801-132 SE1/4SW1/4 sec. 7,

T. 26 N., R. 3 W.

4088888 649001 870 — — — 

Low Wassie 801-135 SE1/4SE1/4 sec. 14, 

T. 26 N., R. 4 W.

4087054 646625 960 — — — 

Low Wassie 801-136 NE1/4SW1/4 sec. 31, 

T. 26 N., R. 3 W.

4082333 649212 920 — — — 

Low Wassie 801-137 SW1/4NE1/4 sec. 36, 

T. 26 N., R. 4 W.

4083082 647730 905 — — — 

Low Wassie 801-138 SW1/4SW1/4 sec. 2, 

T. 26 N., R. 4 W.

4090046 645341 925 — — — 

Low Wassie 801-142 SW1/4SE1/4 sec. 6,

T. 26 N., R. 3 W.

4090167 649584 950 — — — 

Low Wassie 801-143 NW1/4NW1/4 sec. 7, 

T. 26 N., R. 3 W.

4089860 648527 980 — — — 

Low Wassie 801-144 NW1/4NE1/4 sec. 18, 

T. 26 N., R. 3 W.

4088256 649694 853 — — — 

Low Wassie 801-145 NW1/4NE1/4 sec. 18, 

T. 26 N., R. 3 W.

4088289 649446 920 — — — 

Low Wassie 801-146 SW1/4SE1/4 sec. 14, 

T. 26 N., R. 4 W.

4086864 646279 800 — — — 

Low Wassie 801-147 SW1/4SW1/4 sec. 26, 

T. 26 N., R. 4 W.

4083565 645506 955 — — — 

Low Wassie 801-155 NW1/4NW1/4 sec. 23,

T. 26 N., R. 4 W.

4086495 645326 910 — — — 

Low Wassie 801-157 NE1/4SE1/4 sec. 15, 

T. 26 N., R. 4 W.

4087506 644957 1,035 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 47

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –421

 –378

 –452

 –448

 –578

 –585

 –461

 –451

 –444

 –413

 –496

 –604

 –593

 –415

 –440

 –408

 –416

 –438

 –486

 –551

 –510

 –472

 –482

 –434

 –535

 –531

 –675

 –655

 –535

 –519

 –532

 –485

 –570

 –677

 –663

 –504

 –506

 –481

 –485

 –504

 –554

 –638

 –590

 –565

 –634

 –629

 –732

 –729

 –874

 –871

 –738

 –720

 –729

 –686

 –768

 –880

 –864

 –708

 –702

 –678

 –679

 –702

 –749

 –852

 –792

 –757

 –1,060

—

 –1,132

 –1,127

 –1,299

—

 –1,116

 –1,120

 –1,129

 –1,062

 –1,180

 –1,308

 –1,281

 –1,096

 –1,097

 –1,089

 –1,095

 –1,120

 –1,150

 –1,254

 –1,195

 –1,161

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –948

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,139

 –1,155

 –1,311

—

 –1,158

 –1,133

 –1,133

—

 –1,200

—

 –1,303

—

—

 –1,108

—

—

 –1,200

 –1,261

 –1,224

 –1,193

801-111

801-112

801-115

801-116

801-121

801-124

801-125

801-126

801-127

801-132

801-135

801-136

801-137

801-138

801-142

801-143

801-144

801-145

801-146

801-147

801-155

801-157
48 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Low Wassie 801-166 NW1/4NE1/4 sec. 34, 

T. 27 N., R. 4 W.

4092813 644752 953 — — — 

Midridge AC-47 Sec. 18, T. 31 N.,

R. 2 W.

4137622 659164 1,200 — — 895 

Midridge BLM-A047523NW1/4SW1/4 sec. 25, 

T. 31 N., R. 3 W.

4134901 656903 1,277 — 897 642 

Midridge CP-47 Sec. 20, T. 31 N.,

R. 2 W.

4137017 660260 1,236 — — 901 

Midridge CP-48 Sec. 19, T. 31 N.,

R. 2 W.

4137145 659506 1,107 — — 882 

Midridge CP-51 Sec. 20, T. 31 N.,

R. 2 W.

4136816 660555 1,232 — — 922 

Midridge CP-52 Sec. 19, T. 31 N.,

R. 2 W.

4136378 659277 1,239 — 1,014 844 

Midridge CP-57 Sec. 19, T. 31 N.,

R. 2 W.

4137359 658951 1,177 — — 902 

Midridge CP-58 Sec. 19, T. 31 N.,

R. 2 W.

4136797 659441 1,243 — — 868 

Midridge CP-59 Sec. 20, T. 31 N.,

R. 2 W.

4136384 661356 1,197 — — 957 

Midridge CP-63 Sec. 20, T. 31 N.,

R. 2 W.

4136548 660025 1,251 — — 891 

Midridge CP-64 Sec. 20, T. 31 N.,

R. 2 W.

4136925 660744 1,184 — — 954 

Midridge CP-65 Sec. 20, T. 31 N.,

R. 2 W.

4136923 660437 1,236 — — 956 

Midridge CP-68 Sec. 20, T. 31 N.,

R. 2 W.

4136548 660808 1,174 — — 944 

Midridge CP-72 Sec. 20, T. 31 N.,

R. 2 W.

4136961 660602 1,376 — — 1,106 

Midridge CP-74 Sec. 19, T. 31 N.,

R. 2 W.

4137509 659933 1,133 — — 863 

Midridge HA-15 NE1/4NE1/4 sec. 25, 

T. 31 N., R. 3 W.

4135722 658060 1,235 — — 665 

Midridge HA-16 SE1/4SW1/4 sec. 30, 

T. 31 N., R. 2 W.

4134665 658857 1,160 — 840 620 

Midridge HA-17 SE1/4SE1/4 sec. 31, 

T. 32 N., R. 2 W.

4132956 659844 1,010 — — 667 

Midridge HA-30 SW1/4SW1/4 sec. 35, 

T. 31 N., R. 3 W.

4132928 655142 1,190 1,010 — 698 

Midridge HA-32 NE1/4SE1/4 sec. 36, 

T. 31 N., R. 3 W.

4133307 658005 1,215 — — 656 

Piedmont 

Hollow

83W35 SW1/4SW1/4 sec. 3, 

T. 25 N., R. 4 W.

4080664 643885 735 — — –291 
Appendix 1. Summary of Drill-Hole Data for the Study Area 49

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –450

433

205

450

429

482

386

446

424

498

441

508

514

494

659

413

215

211

217

238

206

 –618

 –530

315

109

345

316

381

279

338

317

395

335

406

416

392

559

307

109

98

104

103

54

 –866

 –724

102

 –119

106

94

153

64

121

100

159

115

192

194

162

338

87

 –55

 –74

 –65

 –64

 –96

 –1,250

 –1,098

 –175

 –386

 –165

 –180

 –118

 –221

 –160

 –181

 –113

 –158

 –74

 –60

 –109

34

 –190

 –375

 –396

 –387

 –371

 –401

 –1,252

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –68

—

—

—

—

—

—

—

—

—

 –1,125

 –231

 –386

 –225

 –234

 –170

 –272

 –209

 –231

 –159

 –211

 –87

 –72

 –162

0

 –242

 –379

 –406

 –406

 –385

 –404

 –1,252

801-166

AC-47

BLM-A047523

CP-47

CP-48

CP-51

CP-52

CP-57

CP-58

CP-59

CP-63

CP-64

CP-65

CP-68

CP-72

CP-74

HA-15

HA-16

HA-17

HA-30

HA-32

83W35
50 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Piedmont 

Hollow

82W7 NW1/4NW1/4 sec. 3, 

T. 25 N., R. 4 W.

4081503 643771 745 — — –521 

Piedmont 

Hollow

83W22 NE1/4NW1/4 sec. 3, 

T. 25 N., R. 4 W.

4081749 644408 930 — — — 

Stegall 

Mountain

801-001 Center sec. 14,

T. 27 N., R. 3 W.

4097173 656006 900 — — — 

Stegall 

Mountain

CT-6 NE1/4NW1/4 sec. 18, 

T. 27 N., R. 2 W.

4096442 659806 750 — — — 

Stegall 

Mountain

CT-7 SW1/4SW1/4 sec. 7, 

T. 27 N., R. 2 W.

4098233 658856 829 — — — 

The Sinks HA-26 SE1/4SE1/4 sec. 15, 

T. 31 N., R. 3 W.

4137687 654704 1,210 — — 1,060 

The Sinks HA-27 NE1/4NE1/4 sec. 21, 

T. 31 N., R. 3 W.

4137293 653206 910 — — 865 

The Sinks HA-28 SW1/4 sec. 31,

T. 31 N., R. 3 W.

4133095 649037 1,060 927 — 577 

Van Buren 

North

PD-15-1 NE1/4SE1/4 sec. 15, 

T. 27 N., R. 1 W.

4097519 672564 706 — — — 

Van Buren 

North

SH-12 SE1/4NW1/4 sec. 7, 

T. 28 N., R. 1 W.

4109114 668774 560 — — — 

Van Buren 

North

SH-35 SW1/4NW1/4 sec. 14, 

T. 28 N., R. 1 W.

4108429 674564 580 — — — 

Van Buren 

North

SH-4 NE1/4NW1/4 sec. 21, 

T. 28 N., R. 1 W.

4107269 672564 520 — — — 

Van Buren 

North

CT-3 SE1/4NW1/4 sec. 33, 

T. 28 N., R. 1 W.

4102929 671786 510 — — 255 

Van Buren 

South

PK-16 SW1/4NE1/4 sec. 36, 

T. 26 N., R. 2 W.

4082725 667440 860 — — — 

Van Buren 

South

SF-20 SW1/4SE1/4 sec. 1,

T. 26 N., R. 2 W.

4090123 667281 800 — — –260 

Van Buren 

South

SF-21 NE1/4NW1/4 sec. 4, 

T. 26 N., R. 1 W.

4091724 671846 620 — — –440 

Van Buren 

South

SF-22 SW1/4SW1/4 sec. 3, 

T. 26 N., R. 1 W.

4090165 673037 840 — — –360 

Van Buren 

South

SF-27 NW1/4SW1/4 sec. 11, 

T. 26 N., R. 1 W.

4089328 674773 955 — — –295 

Van Buren 

South

SF-33 NW1/4SE1/4 sec. 10, 

T. 26 N., R. 1 W.

4089105 673772 900 — — –200 

Van Buren 

South

SF-36 SE1/4NW1/4 sec. 10, 

T. 26 N., R. 1 W.

4089548 673441 885 — — –493 

Van Buren 

South

VB-23 Center sec. 2,

T. 26 N., R. 1 W.

4091200 675242 580 — — — 

Van Buren 

South

VB-24 Center sec. 3,

T. 26 N., R. 1 W.

4091054 673603 780 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 51

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

—

 –600

 –271

—

—

—

—

157

 –126

—

—

—

 –160

—

 –422

 –497

 –519

 –589

 –516

 –546

 –744

—

 –873

 –863

 –330

—

—

—

—

45

 –299

—

—

—

 –330

—

 –539

 –599

 –634

 –779

 –737

 –729

 –845

—

 –1,215

 –1,211

 –526

—

—

—

—

 –98

 –430

—

—

—

 –505

 –858

 –682

 –793

 –790

 –838

 –793

 –795

 –878

—

 –1,277

 –1,252

—

—

—

—

—

 –402

 –630

—

—

—

 –795

 –1,305

—

 –1,287

 –1,320

 –1,349

 –1,305

 –1,298

 –1,291

 –1,271

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –650

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,289

 –716

—

—

—

 –632

 –908

 –800

 –838

—

—

 –1,134

—

—

—

—

—

 –1,568

—

 –1,277

 –1,252

 –655

 –1,292

 –770

560

358

 –408

 –658

 –915

 –804

 –860

 –806

 –1,310

 –1,144

 –1,356

 –1,508

 –1,533

 –1,454

 –1,382

 –1,575

 –1,346

82W7

83W22

801-001

CT-6

CT-7

HA-26

HA-27

HA-28

PD-15-1

SH-12

SH-35

SH-4

CT-3

PK-16

SF-20

SF-21

SF-22

SF-27

SF-33

SF-36

VB-23

VB-24
52 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

West Plains 215 SE1/4NW1/4 sec. 35, 

T. 24 N., R. 8 W.

4062889 605677 924 479 — — 

Wilderness MOSS Center SW1/4 sec. 22, 

T. 25 N., R. 2 W.

4075639 663515 ? — — — 

Wilderness 801-007 NE1/4NE1/4 sec. 4,

T. 25 N., R. 2 W.

4081346 663102 780 — — — 

Wilderness 801-26-AL SE1/4SW1/4 sec. 31, 

T. 26 N., R. 2 W.

4081990 658890 975 — — — 

Wilderness 801-53-AK NE1/4SW1/4 sec. 31, 

T. 26 N., R. 2 W.

4082247 658755 985 — — — 

Wilderness 801-62-AY SE1/4SE1/4 sec. 2,

T. 25 N., R. 3 W.

4080317 656527 990 — — — 

Wilderness 801-73 NE1/4NE1/4 sec. 12, 

T. 25 N., R. 3 W.

4080163 658205 990 — — — 

Wilderness 801-105 NE1/4NW1/4 sec. 6, 

T. 25 N., R. 2 W.

4081753 658759 970 — — — 

Wilderness 801-150 SE1/4SW1/4 sec. 31, 

T. 26 N., R. 2 W.

4081869 658775 975 — — — 

Wilderness 88W3 SE1/4NW1/4 sec. 1, 

T. 24 N., R. 3 W.

4071091 656850 810 — — — 

Wilderness 88W11 SW1/4SE1/4 sec. 1,

T. 24 N., R. 3 W.

4070344 657090 760 — — — 

Wilderness 89W22 SE1/4NE1/4 sec. 1,

T. 24 N., R. 3 W.

4071331 657747 830 — — –522 

Wilderness 90W3 SE1/4NW1/4 sec. 6, 

T. 24 N., R. 2 W.

4071061 658582 850 — — –146 

Wilderness 111-A SW1/4NW1/4 sec. 13, 

T. 25 N., R. 2 W.

4078631 666370 800 — — — 

Wilderness 112-A SE1/4SE1/4 sec. 11, 

T. 25 N., R. 2 W.

4078644 666427 680 — — — 

Wilderness 112-B NW1/4SW1/4 sec. 12, 

T. 25 N., R. 2 W.

4079289 666419 830 — — — 

Wilderness 112-C NW1/4NW1/4 sec. 12,

T. 25 N., R. 2 W.

4079925 666447 845 — — — 

Wilderness 112-D SW1/4SW1/4 sec. 12, 

T. 25 N., R. 2 W.

4078868 666431 820 — — — 

Wilderness 112-E SW1/4NW1/4 sec. 12, 

T. 25 N., R. 2 W.

4079533 666447 700 — — — 

Wilderness 112-G SW1/4SW1/4 sec. 12, 

T. 25 N., R. 2 W.

4079031 666439 830 — — — 

Wilderness 113-A SW1/4SW1/4 sec. 1, 

T. 25 N., R. 2 W.

4080561 666447 865 — — — 

Wilderness 122-A NE1/4SE1/4 sec. 11, 

T. 25 N., R. 2 W.

4079121 666104 865 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 53

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

—

—

—

 –430

 –467

 –577

 –572

 –497

—

—

 –871

 –1,015

 –741

—

—

 –577

—

 –580

—

 –567

 –578

 –627

—

—

 –701

 –494

 –517

 –647

 –643

 –567

 –484

 –878

 –931

 –1,153

 –841

 –758

 –728

 –698

 –758

 –705

 –665

 –706

 –724

 –772

—

—

 –920

 –727

 –772

 –885

 –856

 –784

 –687

 –1,132

 –1,239

 –1,407

 –1,151

 –997

 –934

 –903

 –967

 –923

 –864

 –878

 –919

 –984

—

—

 –1,308

 –939

 –1,162

 –1,326

 –1,353

 –1,190

 –1,574

 –1,621

 –1,599

—

—

—

—

—

—

—

—

 –1,325

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –885

—

—

—

—

 –1,173

 –1,173

 –1,070

—

 –1,154

 –1,049

 –1,149

 –1,163

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,450

—

—

—

—

—

 –1,223

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

419

—

 –1,345

 –949

 –1,184

 –1,335

 –1,355

 –1,234

 –895

 –1,590

 –1,640

 –1,760

 –1,654

 –1,327

 –1,175

 –1,075

 –1,295

 –1,158

 –1,051

 –1,157

 –1,165

 –1,425

215

MOSS

801-007

801-26-AL

801-53-AK

801-62-AY

801-73

801-105

801-150

88W3

88W11

89W22

90W3

111-A

112-A

112-B

112-C

112-D

112-E

112-G

113-A

122-A
54 Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri

Appendix 1. Summary of drill-hole data for the study area.—Continued

[Compiled from Kisvarsanyi (1975) and U.S. Bureau of Land Management (BLM) paper files. These data are not available as part of the Missouri Department 

of Natural Resources, Division of Geology and Land Survey well database (http://www.dnr.mo.gov/env/wrc/logmain/index.html) that is maintained by the Water 

Resources Center. Column headings: QUADRANGLE, name of USGS 7.5-minute quadrangle; DRILL HOLE, drill-hole identifier shown on map; LOCATION, section location, or better, in the Public Land Survey System; UTM_NORTH, northing in meters, Universal Transverse Mercator projection, NAD 83, 

Zone 15 North; UTM_EAST, easting in meters, Universal Transverse Mercator projection, NAD 83, Zone 15 North; COLLAR_ELE, collar elevation, in feet 

above mean sea level. Reported elevation of contacts in well, in feet above mean sea level: OR_OG, Roubidoux Formation / Gasconade Dolomite; OG_CE, 

Gasconade Dolomite/Eminence Dolomite; CE_CP, Eminence Dolomite/Potosi Dolomite]

QUADRANGLE DRILL HOLE LOCATION UTM_NORTH UTM_EAST COLLAR_ELE OR_OG OG_CE CE_CP 

Wilderness STH-1 NE1/4SE1/4 sec. 26, 

T. 25 N., R. 2 W.

4074180 666263 920 — — — 

Wilderness STH-2 NE1/4NW1/4 sec. 25, 

T. 25 N., R. 2 W.

4075224 666843 910 — — — 

Wilderness 81W15 NW1/4SW1/4 sec. 3, 

T. 24 N., R. 2 W.

4070881 663195 806 — — –54 

Wilderness 164B SE1/4SE1/4 sec. 31, 

T. 26 N., R. 2 W.

4082196 659597 940 — — — 

Wilderness 164A SW1/4SE1/4 sec. 31, 

T. 26 N., R. 2 W.

4082170 659265 930 — — — 

Winona PK-8 SW1/4 sec. 6,

T. 27 N., R. 3 W.

4100376 648993 1,125 — — — 

Winona PK-12 SE1/4 sec. 1,

T. 27 N., R. 4 W.

4100223 648068 1,110 — — — 

Winona PK-28 NE1/4 sec. 11,

T. 27 N., R. 4 W.

4099442 646285 1,050 — — — 

Winona PK-35 NW1/4 sec. 7,

T. 27 N., R. 3 W.

4099214 649116 995 — — — 

Winona SF-25 SE1/4 sec. 16,

T. 27 N., R. 3 W.

4096434 652828 950 — — — 

Winona SJ77W03 SE1/4SW1/4 sec. 7,

T. 27 N., R. 3 W.

4098424 649281 1,023 — — — 

Winona SJ77W08 SW1/4SW1/4 sec. 36, 

T. 28 N., R. 4 W.

4101491 647263 1,109 — — — 

Winona SJ81W09 SE1/4SE1/4 sec. 36, 

T. 28 N., R. 4 W.

4101513 648268 1,115 — — — 

Winona SJ83W06 NW1/4NW1/4 sec. 17,

T. 27 N., R. 3 W.

4098039 650653 985 — — — 

Winona SJ83W09 SE1/4NE1/4 sec. 27, 

T. 28 N., R. 4 W.

4103756 645156 1,050 — — — 

Winona SJ83W44 SE1/4NW1/4 sec. 27, 

T. 28 N., R. 4 W.

4103773 644544 1,040 — — — 

Winona WN-21 NE1/4 sec. 7,

T. 27 N., R. 3 W.

4099430 649636 1,080 — — — 

Winona WN-22 NW1/4 sec. 8,

T. 27 N., R. 3 W.

4099558 650450 1,060 — — — 

Winona WN-23 NW1/4 sec. 8,

T. 27 N., R. 3 W.

4098911 650750 1,065 — — — 

Winona 27N3W8-1 SW1/4 sec. 8,

T. 27 N., R. 3 W.

4098684 651074 1,055 — 645 342 

Winona 27N3W8-2 SE1/4 sec. 8,

T. 27 N., R. 3 W.

4098108 651880 918 — 643 326 

Winona 27N3W17-1 NE1/4 sec. 17,

T. 27 N., R. 3 W.

4097352 651177 921 — 591 251 

Winona 27N4W1-1 SW1/4 sec. 1,

T. 27 N., R. 4 W.

4100425 647686 1,070 — 655 333 

Winona SH-23 NE1/4NE1/4 sec. 22, 

T. 28 N., R. 4 W.

4105839 645270 871 — — — 
Appendix 1. Summary of Drill-Hole Data for the Study Area 55

[Continued— CP_CDD, Potosi Dolomite/Derby-Doerun Dolomite (Derby-Doerun Dolomite is usage of Missouri Geological Survey, 1979); CDD_CD, DerbyDoerun Dolomite/Davis Formation; CD_CB, Davis Formation/Bonneterre Formation; CB_CL, Bonneterre Formation/Lamotte Sandstone; CD_YV, Davis 

Formation/Mesoproterozoic volcanic rocks; CB_YV, Bonneterre Formation/ Mesoproterozoic volcanic rocks; CB_YG, Bonneterre Formation / Mesoproterozoic 

plutonic rocks; CL_YV, Lamotte Sandstone/ Mesoproterozoic volcanic rocks; CL_YG, Lamotte Sandstone/ Mesoproterozoic plutonic rocks. BOTTOM_ELE, 

elevation of bottom of drill hole, in feet above mean sea level. “?” indicates value is unknown; “—” indicates no data]

CP_CDD CDD_CD CD_CB CB_CL CD_YV CB_YV CB_YG CL_YV CL_YG BOTTOM_ELE DRILL HOLE

 –857

 –867

 –842

 –434

 –447

—

—

—

—

—

—

—

—

—

—

—

—

—

 –91

 –50

 –52

 –194

 –113

—

 –1,052

 –988

 –981

 –579

 –575

—

—

—

—

 –550

 –414

 –281

 –256

 –447

 –200

 –215

—

—

—

 –355

 –400

 –404

 –397

—

 –1,204

 –1,184

 –1,129

 –737

 –734

 –107

 –445

 –557

 –469

 –606

 –601

 –414

 –422

 –618

 –350

 –457

 –278

 –439

 –448

—

 –480

 –491

 –472

—

 –1,614

 –1,788

—

 –1,257

 –1,241

—

—

 –950

 –915

 –1,023

 –830

 –648

—

 –904

 –502

 –668

—

—

 –764

—

—

 –939

 –938

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –382

—

—

—

—

—

—

—

—

—

 –131

 –855

—

—

—

—

—

—

—

—

—

 –467

 –777

—

—

 –639

—

—

 –613

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –658

—

 –967

 –541

 –714

—

—

 –782

—

—

 –989

 –996

—

—

—

—

—

 –1,311

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

—

 –1,667

 –1,831

 –1,630

 –1,419

 –1,322

 –134

 –866

 –967

 –960

 –1,054

—

—

—

—

 –548

 –746

 –483

 –843

 –805

 –423

 –645

 –997

 –1,016

 –622

STH-1

STH-2

81W15

164B

164A

PK-8

PK-12

PK-28

PK-35

SF-25

SJ77W03

SJ77W08

SJ81W09

SJ83W06

SJ83W09

SJ83W44

WN-21

WN-22

WN-23

27N3W8-1

27N3W8-2

27N3W17-1

27N4W1-1

SH-23

Manuscript approved on December 12, 2013

Prepared by the USGS Science Publishing Network

Publishing Service Centers

Edited by James R. Estabrook, Reston

Cartography and graphics by D. Paul Mathieux, Reston

Layout by Caryl J. Wipperfurth, Raleigh

Web support by Angela E. Hall, Reston

For more information concerning this report, contact

David J. Weary

U.S. Geological Survey

926A National Center

Reston, VA 20192
Weary and others—Bedrock Geologic Map of the Spring Valley, West Plains, and Parts of the Piedmont and Poplar Bluff Quadrangles, Missouri—Scientific Investigations Map 3280

ISSN 2329-1311 (print)

ISSN 2329-132X (online)

Printed on recycled paper http://dx.doi.org/10.3133/sim3280